Contribution of combustion Fe in marine aerosols over the northwestern Pacific estimated by Fe stable isotope ratios
- 1Research Institute for Global Change, Japan Agency for Marine-Earth Science and Technology (JAMSTEC), 2-15 Natsushima-cho, Yokosuka, Kanagawa 237-0061, Japan
- 2Department of Earth and Planetary Science, Graduate School of Science, The University of Tokyo, 7-3-1 Hongo, Bunkyo-ku, Tokyo 113-0033, Japan
- 3Center for Global Environmental Research, National Institute for Environmental Studies, 16-2 Onogawa, Tsukuba, Ibaraki 305-8506, Japan
- 4Atmosphere and Ocean Research Institute, The University of Tokyo, 5-1-5 Kashiwanoha, Kashiwa, Chiba 277-8564, Japan
- 5Center for Environmental Science in Saitama, 914 Kamitanadare, Kazo, Saitama 347-0115, Japan
- 6Research Institute for Global Change, JAMSTEC, 3173-25, Showa-machi, Kanazawa-ku, Yokohama, Kanagawa 236-0001, Japan
Correspondence: Minako Kurisu (firstname.lastname@example.org)
The source apportionment of aerosol iron (Fe), including natural and combustion Fe, is an important issue because aerosol Fe can enhance oceanic primary production in the surface ocean. Based on our previous finding that combustion Fe emitted by evaporation processes has Fe isotope ratios (δ56Fe) that are approximately 4 ‰ lower than those of natural Fe, this study aimed to distinguish aerosol Fe sources over the northwestern Pacific using two size-fractionated marine aerosols. The δ56Fe values of fine and coarse particles from the eastern or northern Pacific were found to be similar to each other, ranging from 0.0 ‰ to 0.4 ‰. Most of them were close to the crustal average, suggesting the dominance of natural Fe. On the other hand, particles from the direction of East Asia demonstrated lower δ56Fe values in fine particles (−0.5 ‰ to −2.2 ‰) than in coarse particles (on average −0.02 ± 0.12 ‰). The correlations between the δ56Fe values and the enrichment factors of lead and vanadium suggested that the low δ56Fe values obtained were due to the presence of combustion Fe. The δ56Fe values of the soluble component of fine particles in this region were lower than the total, indicating the preferential dissolution of combustion Fe. In addition, we found a negative correlation between the δ56Fe value and the fractional Fe solubility in air masses from the direction of East Asia. These results suggest that the presence of combustion Fe is an important factor in controlling the fractional Fe solubility in air masses from the direction of East Asia, whereas other factors are more important in the other areas. By assuming typical δ56Fe values for combustion and natural Fe, the contribution of combustion Fe to the total (acid-digested) Fe in aerosols was estimated to reach up to 50 % of fine and 21 % of bulk (coarse + fine) particles in air masses from the direction of East Asia, whereas its contribution was small in the other areas. The contribution of combustion Fe to the soluble Fe component estimated for one sample was approximately twice as large as the total, indicating the importance of combustion Fe as a soluble Fe source despite lower emissions than the natural. These isotope-based estimates were compared with those estimated using an atmospheric chemical transport model (IMPACT), in which the fractions of combustion Fe in fine particles, especially in air masses from the direction of East Asia, were consistent with each other. In contrast, the model estimated a relatively large contribution from combustion Fe in coarse particles, probably because of the different characteristics of combustion Fe that are included in the model calculation and the isotope-based estimation. This highlights the importance of observational data on δ56Fe for size-fractionated aerosols to scale the combustion Fe emission by the model. The average deposition fluxes of soluble Fe to the surface ocean were 1.4 and 2.9 nmol m−2 d−1 from combustion and natural aerosols, respectively, in air masses from the direction of East Asia, which suggests that combustion Fe could be an important Fe source to the surface seawater among other Fe sources. Distinguishing Fe sources using the δ56Fe values of marine aerosols and seawater is anticipated to lead to a more quantitative understanding of the Fe cycle in the atmosphere and surface ocean.
Iron (Fe) is an essential element for marine biota. Although Fe is the fourth most abundant element in the Earth's crust (Taylor, 1964), the concentration of Fe in the surface ocean can be as low as 0.05 nM (Martin et al., 1989; Schlitzer et al., 2018). In high-nutrient low-chlorophyll (HNLC) regions, the deficiency of bioavailable Fe is considered one of the main limiting factors of primary production of phytoplankton (Martin et al., 1994; Martin and Fitzwater, 1988; Moore et al., 2013). Phytoplankton activity has a major impact on the biogeochemical cycles of various elements, such as carbon, nitrogen, sulfur, and other trace elements (Charlson et al., 1987; Falkowski et al., 1998). In particular, ocean Fe fertilization plays an important role in the uptake of carbon dioxide (CO2), decreasing the partial pressure of CO2 in the atmosphere and positively affecting the global climate (Ciais et al., 2014; Falkowski et al., 1998). Therefore, understanding how Fe is supplied to the surface ocean is an important issue.
Atmospheric aerosols, mainly in the form of mineral dust, are considered to be one of the main components that supply Fe to the surface ocean. Mineral dust transported from East Asia has been recognized as an important supplier of Fe to the surface of the North Pacific Ocean, including HNLC regions, although there is significant seasonal variation in the flux of mineral dust (Duce et al., 1991; Jickells, 2005; Uematsu et al., 1983). In addition to aerosols, the dissolution of Fe from coastal sediments (Lam and Bishop, 2008; Nishioka et al., 2013; Nishioka and Obata, 2017) and hydrothermal vents (Fitzsimmons et al., 2017; Tagliabue et al., 2010) has been suggested to be an important source of dissolved Fe in the surface ocean.
A great deal of attention has been paid to combustion Fe in aerosols as an important source of Fe in the surface ocean (Ito et al., 2019; Kurisu et al., 2016b, 2019; Sholkovitz et al., 2009). The amount of Fe emitted globally from combustion sources is estimated to be 2.1 ± 0.5 Tg Fe yr−1, which is an order of magnitude smaller than the mineral dust emission (72 ± 43 Tg Fe yr−1; Myriokefalitakis et al., 2018). However, combustion Fe is considered to be an important source of soluble Fe, which is thought to be easily bioavailable because of its high Fe fractional solubility in comparison with that of Fe in mineral dust (Schroth et al., 2009; Sholkovitz et al., 2009; Takahashi et al., 2013). Moreover, the fertilizing effect of combustion Fe has been increasingly examined in ocean biogeochemistry models, some of which showed that combustion Fe is more efficient at enhancing marine productivity than Fe from mineral dust sources (Hamilton et al., 2020; Ito et al., 2020). It is, however, still a major challenge to quantitatively understand and predict the high variability and complex aerosol chemistry of combustion Fe sources and the diverse marine biogeochemical responses (Ito et al., 2021a).
The fractional Fe solubility is defined as follows:
where T-Fe and S-Fe are the concentrations of acid-digested (total) and soluble Fe, respectively (Buck et al., 2006; Morton et al., 2013). The fractional Fe solubility of aerosols is controlled by various factors, such as (i) the size or surface area of the particles (Baker and Jickells, 2006), (ii) the occurrence of atmospheric reactions with various acids (of both natural and anthropogenic origin) and photochemical reactions during transport (Chen and Grassian, 2013; Ito et al., 2019; Takahashi et al., 2011), and (iii) differences in the chemical forms of Fe. Variations in the chemical form of Fe depend heavily on the source of Fe. Iron in mineral dust is mainly found in the form of crystalline Fe oxides or Fe in aluminosilicates, which typically exhibit very low fractional solubility (approximately 0.1 % to 1 %). Combustion aerosols contain more labile forms of Fe, such as Fe (hydr)oxides, aggregates of nano-sized Fe oxides, and Fe sulfates. They are highly soluble (up to 80 %) or more easily solubilized by atmospheric reactions (Schroth et al., 2009; Takahashi et al., 2011). However, the relative importance of these factors remains unclear, particularly in the marine atmosphere.
The contribution of combustion and natural Fe in aerosols has been estimated in various modeling studies (e.g., Ito et al., 2019; Luo et al., 2008; Matsui et al., 2018; Myriokefalitakis et al., 2018), the results of which suggest the important contribution of combustion Fe to soluble Fe deposition (up to 90 % depending on areas and models). The parameterizations used in these studies differ depending on the model used, especially in terms of the amount of Fe emitted from various sources, the Fe solubility at emission (particularly for combustion Fe), and the solubilization processes that occur during atmospheric transport, which lead to different results. Myriokefalitakis et al. (2018) compared the results of several model calculations with observational data and reported several problems, including (i) different estimations of the contribution of combustion Fe to remote ocean regions among the various models, (ii) an overestimation of the concentration of atmospheric Fe near dust source regions, and (iii) an underestimation of the Fe concentrations in remote oceanic regions compared with observations. They claimed that some uncertainties remain, such as the relative contribution of combustion and dust Fe to the soluble Fe that is present over remote oceanic regions, aerosol size distributions, and atmospheric processing under the presence of combustion Fe and anthropogenic pollutants. These model studies usually evaluate their results by comparing the estimated Fe concentrations and solubilities with observed T-Fe and S-Fe concentrations. However, this method cannot be used to directly compare the fractions from different sources of Fe.
The iron stable isotope ratio can be used to distinguish Fe from different sources (Dauphas et al., 2017). It is reported as the value of δ56Fe relative to a standard material (IRMM-014, Institute for Reference Material and Measurements) using the following equation:
The average δ56Fe value of mineral dust is −0.01 ± 0.08 ‰, which is similar to that of terrestrial igneous rocks or soil (0.00 ± 0.05 ‰; Beard et al., 2003). In contrast, combustion Fe has a comparatively low δ56Fe value (as low as −4 ‰), which is a result of the kinetic isotope fractionation that occurs during evaporation under high-temperature conditions (>800 ∘C), such as fossil fuel combustion, industrial production of metals, and vehicle emissions, among others (Kurisu et al., 2016a, b, 2019; Kurisu and Takahashi, 2019). Combustion Fe can be distinguished from natural Fe, which is not possible from the observed T-Fe and S-Fe concentrations (Meskhidze et al., 2019), by using the isotope ratio as a tracer. Ascertaining the source of Fe in seawater using δ56Fe values has been conducted in several studies, with aerosols considered to be an important source of Fe, even in seawater (Conway and John, 2014; Labatut et al., 2014; Pinedo-González et al., 2020). Pinedo-González et al. (2020) observed low δ56Fe signals in the surface seawater of the North Pacific that may have originated from combustion Fe in East Asia. However, the δ56Fe of the aerosols was not measured during the same period in this study, and there have been few reports concerning the collection of Fe isotope ratios from aerosols over the ocean. Conway et al. (2019) reported the Fe isotope ratios of marine aerosols over the North Atlantic and suggested that the total (acid-digested) aerosols contained a δ56Fe value close to the crustal value, whereas soluble aerosols had low δ56Fe values due to the presence of combustion Fe with low δ56Fe and high fractional Fe solubility. Our previous study reported a limited dataset of δ56Fe values of two size-fractionated marine aerosols collected near the Japanese coast, which indicated that acid-digested fine particles had considerably lower values of δ56Fe than coarse particles because of the presence of combustion Fe in fine particles (Kurisu et al., 2016b). However, more data relating to the δ56Fe of aerosols collected in the northwestern Pacific, including the open ocean, are required to gain further insights into the atmospheric mixing among air masses of combustion Fe of various origins. Furthermore, size-fractionated aerosol sampling would make it possible to discuss the influence of combustion Fe more clearly because of the difference in the size distribution of combustion and natural aerosols.
In this study, two size-fractionated aerosol samples were collected in the northwestern Pacific, to which aerosols from the direction of East Asia can be transported and in which the influence of combustion Fe can be observed. In this study, we aimed (i) to discuss the contribution of combustion and natural Fe to marine aerosols based on Fe isotope ratios and (ii) to evaluate the importance of combustion Fe as a controlling factor of fractional Fe solubility by combining data relating to the fractional solubility, Fe species, and Fe isotope ratios. We also compared the fraction of combustion Fe in marine aerosols estimated using Fe isotope data with that estimated by a model calculation, with the aim of discussing the applicability of Fe isotopes to improving process-based estimations.
2.1 Sample collection
Marine aerosol samples were collected during the R/V Hakuho Maru KH-13-7 (12 December 2013 to 11 February 2014, samples 13-a to 13-e, Table S1) and KH-14-3 cruises (24 June to 9 August 2014, samples 14-A to 14-O, Table S2) around the northwestern Pacific (Fig. 1). The aerosol sampling was conducted on the compass deck (13 m above sea level). Two size-fractionated aerosols (finer and coarser than 2.5 µm) were collected on polytetrafluoroethylene (PTFE) filters (ADVANTEC, PF040, 90 mm ∅) using a high-volume virtual dichotomous air sampler (Kimoto, Model AS-9, Japan) at a mean flow rate of 15 m3 h−1. The sampler was automatically controlled by a wind sector that was operated only when the relative wind direction ranged from −90 to 90∘ from the perspective of the bow and the relative wind speed was more than 1 m s−1. The typical sampling duration was 3 d, and the mean volume of filtered air was approximately 720 m3. The samples were stored at −18 ∘C until chemical analysis could be conducted. Filter blanks were checked by setting filters on the sampler without running.
2.2 Acid digestion of aerosol samples
Acid digestion of the aerosol samples was conducted to determine the total concentrations of Fe and other trace elements, including titanium (Ti), vanadium (V), and lead (Pb). All the procedures were conducted in a HEPA-filtered (SS-MAC15, Air Tech, Japan) clean bench in a class-10000 clean room. Perfluoroalkoxy (PFA) vials (Savillex, USA) and low-density polyethylene (LDPE) bottles (Nalgene, Thermo Fisher Scientific, Germany) were used for sample processing and storage of the solutions, respectively. All equipment was preliminarily washed by sequential soaking overnight in warm 3 mol L−1 nitric acid (HNO3, for the electronics industry, FUJIFILM Wako Pure Chemical Corp., Japan), warm 3 mol L−1 hydrochloric acid (HCl, for the electronics industry, FUJIFILM Wako Pure Chemical Corp., Japan), and ultrapure water (>18.2 MΩ cm, Milli-Q, Millipore GmbH, Japan). All acids used for the digestion, including HNO3, HCl, and hydrofluoric acid (HF), were Tamapure AA-100 grade (each metallic impurity less than 100 pg mL−1, Tama Chemical Co., LTD., Japan). Approximately of each sample filter was digested in a closed PFA vial by adding 2 mL of 15.3 mol L−1 HNO3, 2 mL of 9.3 mol L−1 HCl, and 1 mL of 22 mol L−1 HF. The sample in the vial was then heated at 150 ∘C for 1 d and evaporated to near dryness. A 1 mL volume of 15.3 mol L−1 HNO3 was then added, and the sample was again heated at 150 ∘C for one day and evaporated to near dryness. The residue was then redissolved in an appropriate amount of 0.3 mol L−1 HNO3 for concentration analysis, which was conducted using inductively coupled plasma quadrupole mass spectrometry (ICP-QMS, Agilent 7700, Agilent, Japan). For the measurement of 56Fe, helium collision cell mode was used to remove ArO interference. Acid digestion was conducted just once for each sample as the quantity of each sample was limited. The effectivity of the measurement was confirmed by measuring the certified reference material CJ-2 (simulated Asian mineral dust, Table S3; Nishikawa et al., 2000). The average concentration of each element in the blank filter was subtracted from those in the samples. The Fe concentration in the blank filter was 2.5 ± 0.6 ng Fe per cm2 of filter. Coarse particles were collected on the center part of the filter (5 % of the filter area), whereas finer particles were collected on the outer part of the filter (95 % of the filter area). Thus, the blank Fe concentration per the same volume of air was larger in fine particles than in coarse particles. Assuming that the total volume of filtered air was 720 m3, the detection limits of Fe mass concentrations were approximately 1 × 10−2 and 2 × 10−1 ng m−3 for coarse and fine particles, respectively. Detection limits of the other elements were 4 × 10−3, 3 × 10−5, and 2 × 10−4 ng m−3 for coarse particles of Ti, V, and Pb, respectively, and 7 × 10−2, 5 × 10−4, and 3 × 10−3 ng m−3 for fine particles of Ti, V, and Pb, respectively.
The enrichment factor (EF), which is useful in understanding the impact of anthropogenic materials relative to crustal materials, was calculated according to the following equation:
where M is the concentration of the target element. The crustal value of each element was obtained from Taylor (1964).
2.3 Fractional Fe solubility
The fractional Fe solubility was calculated according to Eq. (1), for which soluble Fe (S-Fe) was evaluated via a leaching experiment. We applied the “flow-through extraction” method to solubilize the labile Fe component (Buck et al., 2006). For this method, extraction was conducted by pouring 100 mL of ultrapure water onto a sample filter in a pre-washed PTFE filter holder (47 mm single-stage filter assembly, Savillex, USA) equipped with a pre-washed 0.4 µm polycarbonate filter. A vacuum was applied during the extraction. The solution was collected in an LDPE vial and acidified with HNO3 to avoid precipitation of the iron hydroxides, then evaporated in a PFA vial. The residue was then redissolved in 0.3 mol L−1 HNO3 for concentration analysis with ICP-QMS. The filter blank was 0.018 ± 0.003 ng Fe per cm2 of filter, which was subtracted from each sample concentration. Although our previous studies applied different extraction methods, the flow-through method was applied in this study to compare the results with other studies of marine aerosols (e.g., Buck et al., 2006; Conway et al., 2019; Morton et al., 2013; Shelley et al., 2018).
2.4 Iron speciation
The average Fe species of each sample was determined by Fe K-edge X-ray absorption fine structure (XAFS) spectroscopy at beamline BL-12C of the Photon Factory (PF), KEK (Ibaraki, Japan). The methods used were similar to those of previous studies (Kurisu et al., 2019; Takahashi et al., 2011). The X-ray was monochromatized using an Si(111) double-crystal monochromator and focused using a bent cylindrical mirror. The energy resolution was eV. The higher-order harmonic waves were eliminated using Ni-coated double mirrors. The reference spectra were recorded in transmission mode, whereas the sample spectra were recorded in fluorescence mode by placing the samples 45∘ from the incident beam. The Fe Kα (6.41 keV) line was detected using either a 19-element germanium solid-state detector or a 7-element silicon drift detector (SDD). X-ray absorption near-edge structure (XANES) spectra from 7.000 to 7.250 keV were recorded. Spectra were normalized at 7.200 keV, and linear combination fitting was conducted in the energy range of 7.110 to 7.160 keV using REX2000 software (Rigaku Co., Ltd., Japan). For the energy calibration, the pre-edge peak energy of hematite was set to 7.112 keV. The quality of the fitting was checked using the parameter R, which is defined using
where Iobs(E) and Ical(E) are the X-ray absorbance of the original and calculated spectra, respectively, at a certain energy. The fitting errors for the fraction of the reference species were calculated as the difference in the fraction when the R value is twice the best-fitted value (Kodama et al., 2006). The error of each fitting was within 10 %. The samples contained just a small amount of Fe, so aerosol particles were mounted on a Kapton tape from the sampling filter to gather the particles at one point.
The micro-XAFS combined with X-ray fluorescence mapping (µ-XRF-XAFS) was conducted at BL-4A and BL-15A1 of the PF for analysis of the narrow spot speciation and to check the distribution of Fe and other elements. A 7.50 keV or 3.00 keV (for sulfur mapping) incident beam was used for elemental mapping. The Fe Kα (6.41 keV), potassium (K) Kα (3.31 keV), and sulfur (S) Kα (2.31 keV) lines were detected using a single-element SDD. The incident beam sizes at beamlines BL-4A and BL-15A were approximately 4 × 5 and 20 × 20 µm2, respectively. Note that the beam sizes were larger than the fine particles (with aerodynamic diameters of <2.5 µm); therefore, each spot could contain several particles. All of the aerosol sample spectra were recorded using the fluorescence mode of the SDD.
2.5 Iron isotope analysis
The sample preparation methods that were used for isotope analysis were the same as those described in Kurisu et al. (2019) except for the method used to separate Fe with an anion exchange resin (AG-MP-1, 100–200 mesh, Bio-rad). The amount of resin was reduced to lower the Fe contamination from the resin, which can be problematic for the analysis of small amounts of Fe, such as those found in marine aerosol samples. A microcolumn with a diameter of 2 mm was prepared with a heat-shrink PTFE tube (inner diameter: in., 4:1 heat shrink, Zeus Inc.), according to the method described by John and Adkins (2010). A frit was made of polyethylene. Approximately 20 µL of resin was used for each separation, with the resin reaching a height of approximately 5 to 7 mm. The column was washed with 3.0 mol L−1 HCl prior to use. The resin was washed by sequential soaking for 1 week in 0.5 mol L−1 HNO3 and 0.5 mol L−1 HCl, respectively, with rinsing with ultrapure water between steps. The procedures that were used for the column separation are described in Table S4 and were modified from the method proposed by Conway et al. (2013). The procedure blank was 0.30 ± 0.15 ng Fe (1 SD, n=3), which was more than 100 times lower than the amount of Fe in the sample. The recovery rate of Fe was 101 ± 5 %, and the efficient removal of other elements was confirmed (Fig. S1).
Iron isotope analysis was conducted using a multi-collector ICP-MS (MC-ICP-MS, Neptune Plus, Thermo Fisher Scientific, Germany). The methods used for the analysis were also the same as those described in Kurisu et al. (2016b, 2019). A standard-sample bracketing method was adopted, with Cu doping as an external standard for mass bias correction using the exponential law (Albarede et al., 2004). The medium-resolution mode was used to resolve any argide interference (mainly 40Ar14N+, 40Ar16O+, 40Ar16OH+, and 40Ar18O+). Data were obtained in dynamic mode with the Faraday cup setting to monitor the isotopes of 52Cr, 54Fe, 56Fe, 57Fe, and 58Fe in one cycle and 63Cu and 65Cu in another. Iron isotope ratios were reported as the ratio of 56Fe to 54Fe according to Eq. (2). The ratio of 57Fe to 54Fe was used to check the reliability of the measurement in a three-isotope plot. The interference of 54Cr with 54Fe was less than 0.1 mol % in each sample and was corrected using 52Cr 54Cr = 0.0282 (Beard et al., 2003). By comparing the δ56Fe in a Cr-free standard solution with the same solution under Cr doping (54Cr 54Fe up to 0.01 in mol fraction), it was confirmed that no bias was observed between them. The Fe concentration was adjusted to 500 µg L−1 for the isotope measurement. As the amount of Fe in each sample was small, the volume of the samples was low; therefore, limited iterations of the isotope measurements could be conducted.
Since the aerosol sampling filters contained some blank Fe, the δ56Fe for each sample was corrected by measuring the δ56Fe of a blank filter (δ56Feblank, 0.13 ± 0.07 ‰, n=3). Based on the blank Fe to total Fe ratios (Tables S4 and S5), the δ56Fe of the sample Fe (δ56Fesample) was calculated according to the following mixing equation:
Some samples were not available because the blank Fe was high (more than approximately 40 % of the total Fe) or because the amount of sample Fe was too small. In other samples, δ56Femeasured and δ56Fesample were similar in their range of error (Tables S4 and S5); thus, this correction did not seriously affect the results and discussion of the isotope data. Although the Fe isotope and speciation data for samples 14-N and 14-O have already been reported in Kurisu et al. (2016b), they were combined with the other newly obtained data in this study.
2.6 Atmospheric chemical transport model
This study compared the results of the fraction of combustion Fe in aerosols with those estimated by the Integrated Massively Parallel Atmospheric Chemical Transport (IMPACT) model (Ito et al., 2021b; Rotman et al., 2004). Simulations were performed for the same period as the aerosol sampling using a horizontal resolution of 2.0∘ × 2.5∘ and 47 vertical layers. The IMPACT model categorized the Fe origins into mineral dust (Comp 1), oil combustion (ship emission, Comp 2), anthropogenic combustion on land (mainly coal combustion and the iron and steel industry, Comp 3), and biomass burning (Comp 4) for four distinct aerosol size bins (0.1–1.26, 1.26–2.5, 2.5–5, and 5–20 µm in diameter). We compared the sum of Comp 2 and Comp 3 with the isotope-based estimation for fine (i.e., the sum of bins 1 and 2) and coarse (i.e., the sum of bins 3 and 4) particles. Although biomass burning (Comp 4) may contain a combustion Fe source, we did not include it for the comparison. This is because the Fe emitted by biomass burning does not yield δ56Fe values that are as low as those from other anthropogenic combustion sources, which is likely due to strong influences by mineral dust aerosols entraining into the atmosphere during biomass burning (Kurisu and Takahashi, 2019).
3.1 Sources of aerosols
A 7 d backward trajectory analysis was conducted using the Hybrid Single-Particle Lagrangian Integrated Trajectory (HYSPLIT) model to discern the source of the air masses (Stein et al., 2015), which were then divided into three broad groups (Fig. 2). The first group was mainly transported from the direction of East Asia via westerly winds and corresponded to samples 13-a, 13-d, 13-e, 14-A, 14-N, and 14-O (group I, Fig. 2a). Winter samples (KH-13-7) were transported longer distances from the Eurasian continent, whereas summer samples (KH-14-3) passed over Japan or the western part of the Pacific. They possibly contained aerosols emitted both by natural and anthropogenic sources. The second group was from the central and eastern Pacific and comprised samples 13-b, 13-c, 14-B, 14-C, 14-D, 14-E, 14-F, 14-G, 14-H, and 14-I (group II, Fig. 2b). The third group was from the northern North Pacific and was composed of samples 14-J, 14-K, 14-L, and 14-M (group III, Fig. 2c).
The Fe concentration was significantly affected by the source of air masses. The bulk Fe concentrations (fine + coarse) were 2.6 to 41.8 ng m−3 in the vicinity of East Asia (group I, 19.8 ± 13.8 (SD) ng m−3). Among the group I samples, KH-13-7 samples showed high concentrations even when the sampling points were relatively far from the Japanese coast. This is possibly because they contained a large number of particles transported from the Eurasian continent. Samples in groups II (1.97 ± 1.48 ng m−3) and III (1.78 ± 0.68 ng m−3) showed Fe concentrations of less than 5 ng m−3 (Fig. 3a, Tables S4 and S5). The concentrations were relatively low, even in group I, compared with concentrations reported from previous studies conducted in the Pacific (1 to 800 ng m−3; Buck et al., 2006, 2019; Duce and Tindale, 1991; Sakata et al., 2018), in which more than 100 ng m−3 of Fe was often observed during dust events from East Asia. Therefore, it is assumed that our samples were not affected by a large dust event from the continent. Samples 14-G and 14-H showed Fe concentrations that were slightly higher than the samples from neighboring locations, especially in the coarse particles, which may be derived from the Hawaiian islands. The Fe concentrations of the fine particles in the group III samples were below the detection limit because of a smaller quantity of Fe in the samples than that in the blank.
The concentrations of other elements are also shown in Fig. S2. Titanium (Ti), which is abundant in the Earth's crust, showed similar concentration distributions as those of Fe (Fig. S2a). In addition, V and Pb, which originate mainly from oil and coal combustion (e.g., Nriagu and Pacyna, 1988; Zhang et al., 2009), respectively, were also found at high concentrations near East Asia (group I, Fig. S2b and c) and were at especially high concentrations in the fine particles, suggesting the significant influence of material from combustion sources. To further investigate the sources of the aerosols, the EF values were also compared. An EF value of more than 10 usually suggests a significant influence of anthropogenic materials (Buck et al., 2019; Shelley et al., 2015). The EFFe values were 0.4 to 3 (Fig. 4a), although several of the samples showed large errors. The average values (± SD) were 1.52 ± 0.48 (group I of the coarse particles), 1.27 ± 0.56 (group II of the coarse particles), 0.98 ± 0.08 (group III of the coarse particles), 1.23 ± 0.35 (group I of the fine particles), and 1.20 ± 0.73 (group II of the fine particles). Their values were close to 1, suggesting that Fe mainly originated from crustal sources. When we compared the difference among the groups, a significant difference between groups I and III for the coarse particles was found and was not found in the other groups (by the Wilcoxon rank-sum test, significant difference at p<0.05). The higher EFFe value of the coarse particles of group I than group III indicates that group I contained Fe-rich particles. Considering that the high EFFe values were observed near the Japanese coast (14-A and 14-O), coarse particles of group I possibly contained some amount of anthropogenic Fe emitted by industrial activities in Japan, in addition to crustal materials. The influence of combustion Fe in the other groups was not clear only from the EFFe. EFPb values were more than 10 for most of the samples, especially in the fine particles, indicating that most of the samples contained anthropogenic Pb (Fig. 4c). The EFPb of the fine particles in group I (EFPb=764 ± 739 – SD) was higher than that of the other samples (203 ± 142 and 161 ± 23 for groups II and III, respectively), especially in the winter (KH-13-7, EFPb=1289 ± 727), which is indicative of a large influence from coal combustion in East Asia. EFV values varied from 1.7 to 840, with higher EFV values in fine particles (EFV=74 ± 185) than in coarse particles (Fig. 4b, EFV=4.92 ± 3.82). The EFV values of the fine particles in the group III samples (EFV=370 ± 320) were more than 100, which is higher than the other samples, but this was not the case for Pb. Because V is mainly emitted during the combustion of heavy oil, the group III samples were likely influenced by ship emissions, which is plausible considering that many ships traverse the northern Pacific (https://www.marinetraffic.com, last access: 30 May 2021).
3.2 Fractional Fe solubility
The fractional Fe solubility varied from 0.1 % to 23 %, with the highest solubility observed in the fine particles in 13-c (Fig. 3c). The fractional solubilities were in a similar range as those observed in other studies conducted in the North Pacific (Buck et al., 2006; Wang and Ho, 2020; Wu et al., 2007). The average fractional Fe solubility (± SD) of each group was 1.46 ± 1.51 %, 1.13 ± 1.62 %, and 2.22 ± 1.43 % for the coarse particles of groups I, II, and III, respectively, whereas it was 5.89 ± 4.04 % and 4.52 ± 6.69 % for the fine particles of groups I and II, respectively. Although there were no clear differences in the fractional solubilities of the different air mass groups (by the Wilcoxon rank-sum test, significant difference at p<0.05), fine particles often showed a higher soluble Fe concentration and fractional Fe solubility than the coarse particles of the same sample, which is consistent with previous reports (Kurisu et al., 2016b; Ooki et al., 2009). A scatter plot of the atmospheric Fe concentration and the fractional Fe solubility also showed a similar trend as previous studies, with high fractional solubilities obtained when Fe concentrations were low (Fig. S3; Mahowald et al., 2018; Sholkovitz et al., 2009, 2012); the reason for this trend will be discussed later.
3.3 Iron species
The difference in the peak energies of the XANES spectra reflects the oxidation state of Fe. The higher peak energy of the Fe K-edge XANES spectrum corresponds to a larger amount of ferric species, as seen in the reference materials (Fig. 5a; Berry et al., 2003; Maggi et al., 2018). The peak energies of some of the samples (such as the coarse particles of sample 13-a) were approximately 7.126 keV, whereas those of other samples (such as the fine particles of 13-a) were higher in the range between 7.126 and 7.131 keV, indicating that they contained a larger fraction of ferric species. The spectra of the samples were successfully fitted by linear combination to those described by the reference samples. The ratios obtained by fitting are tabulated in Table S7. For simplification, the main Fe species were categorized into Fe-containing silicates (fayalite, weathered biotite, chlorite, and illite with various Fe(II) fractions) and Fe (hydr)oxides (magnetite, goethite, hematite, and ferrihydrite; Fig. 5e), considering that Fe-containing silicates are of natural origin, whereas Fe (hydr)oxides can be of both natural and combustion origin. The fraction of each species in coarse and fine particles was similar within a range of approximately 10 % error in most of the group II samples from the central and eastern Pacific, whereas the fractions of (hydr)oxides in the group I samples from the direction of East Asia and some of the group II samples were higher in fine particles than in coarse particles.
The presence of Fe-containing silicates was confirmed by spot analysis of some of the samples (13-a, 13-b, 14-N, and 14-O) using µ-XRF-XAFS. For example, there were several Fe-concentrated spots in the coarse and fine particles (Figs. S4–S7). These were Fe-containing aluminosilicates, such as weathered biotite, illite, and chlorite, the presence of which was also supported by the correlation with the intensity of potassium (K) in the µ-XRF maps (Fig. S4b and d). These species were also previously observed in aerosols that were collected in East Asia (Kurisu et al., 2016b; Takahashi et al., 2011), suggesting the presence of mineral dust from East Asia. The presence of Fe (hydr)oxides was also observed in the spot analysis, with some particles containing ferrihydrite, goethite, magnetite, and hematite (Figs. S5, S6, and S7). Ferrihydrite was often found in the fine particles within sample 13-c that was collected in the open ocean, which was also consistent with the bulk XANES analysis (Fig. S6). In addition to Fe-containing aluminosilicates and Fe (hydr)oxides, Fe(III) sulfate, a highly soluble Fe species, was also observed in the coarse particles of sample 13-c, although it was not detected as a main Fe species in the bulk analysis. The presence of Fe(III) sulfate was supported by the co-presence of Fe and S (spots 5 and 6 in Fig. S5b).
3.4 Iron isotope ratios
Negative δ56Fe values ranging from −0.45 ‰ to −2.16 ‰ were observed in the fine particles of group I (on average −1.10 ± 0.63 ‰ – SD) in air masses from the direction of East Asia (Fig. 6, Tables S4 and S5). These values were much lower than those observed for the coarse particles (on average −0.02 ± 0.12 ‰). The δ56Fe values were particularly low in the fine particles of samples collected in the vicinity of the Japanese coastline (13-a, 14-N, and 14-O). The bulk (coarse + fine) δ56Fe values calculated from the Fe concentration and δ56Fe of each size fraction ranged from −0.07 ‰ to −0.91 ‰ (Tables S5 and S6, on average −0.45 ± 0.32 ‰); this is considerably lower than the values obtained from North American or European air masses in the North Atlantic, which reached as low as −0.16 ‰ (Conway et al., 2019), suggesting an important contribution of aerosols with low δ56Fe values in the North Pacific aerosols. These low δ56Fe values may have originated from combustion Fe, which is discussed in more detail later.
In air masses from the central, eastern, or northern Pacific (in groups II and III), the δ56Fe values of both the coarse (on average 0.25 ± 0.14 ‰ and 0.14 ± 0.10 ‰ for groups II and III, respectively) and fine (on average 0.23 ± 0.17 ‰ for group II samples and 0.43 ± 0.17 ‰ for 14 L in group III) particles were close to or higher than 0 ‰. The coarse and fine particles in each sample yielded similar δ56Fe values to each other, although the δ56Fe of the fine particles in some samples could not be measured due to the low quantity of sample Fe compared with blank Fe. Most of the values were close to the crustal value, whereas the δ56Fe of some samples was higher than the crustal average, reaching as high as 0.43 ‰, which did not correspond to typical crustal values (−0.3 ‰ to 0.3 ‰, Johnson et al., 2003; Majestic et al., 2009; Mead et al., 2013).
The coarse and fine particles in sample 13-e and the fine particles of sample 13-d contained sufficient soluble Fe for isotope analysis to be conducted (Table S5). The resulting values were −0.27 ± 0.03 ‰, −1.14 ± 0.03 ‰, and −2.23 ± 0.04 ‰ for the coarse particles in 13-e, fine particles in 13-e, and fine particles in 13-d, respectively, which were lower than those of the acid-digested (total) Fe (0.10 ± 0.14 ‰, −0.47 ± 0.18 ‰, and −0.45 ± 0.28 ‰, respectively), especially for fine particles (Table S5). These low values in fine particles were due to the preferential dissolution of components with a low δ56Fe value (i.e., combustion Fe). It should be noted that these lower δ56Fe values could be due to kinetic isotope fractionation taking place during the partial dissolution of a single phase (Revels et al., 2015; Wiederhold et al., 2006). However, such fractionation would become large as the fractional Fe solubility decreases, which was not the case with our results; the difference between the δ56Fe values in the total and soluble fractions of the samples was greater when the fractional Fe solubility was large (Tables S5 and S6; Fig. 3c). It is possible that the soluble component of the coarse particles of 13-e had δ56Fe lower than that of the total due to kinetic isotope fractionation. However, the low δ56Fe values, especially in terms of the fine particles, cannot be explained solely by kinetic isotope fractionation, and the component with a low δ56Fe value (combustion Fe) must have dissolved preferentially. The bulk (coarse + fine) δ56Fe value of −0.79 ‰ was calculated for 13-e from the concentration and δ56Fe of soluble Fe in each size component, and although the δ56Fe of the coarse particles in 13-d was not measured, the bulk (coarse + fine) δ56Fe value was probably close to the δ56Fe of the fine particles (−2.23 ‰), as most of the soluble Fe in sample 13-d was from fine particles (Fig. 3b and Table S5). These calculated bulk δ56Fe values were in a similar range as or lower than those observed previously in the North Atlantic (reaching as low as −1.6 ‰, Conway et al., 2019), indicating the significance of low-δ56Fe components (i.e., combustion Fe) in the northwestern Pacific.
4.1 Source apportionment of Fe in aerosols based on δ56Fe values
4.1.1 Do the negative δ56Fe values in fine particles mean they are of combustion origin?
The Fe isotope analysis indicated that low δ56Fe values were observed in the fine particles within air masses from the direction of East Asia. To check if the low δ56Fe values were a result of the presence of Fe from anthropogenic combustion, the relationship between δ56Fe and the concentration of anthropogenic constituents was explored (Fig. 7). The δ56Fe values were weakly correlated with EFPb, EFV, and the concentration of carbon monoxide, which indicated that aerosols that contained anthropogenic materials also contained Fe with low δ56Fe values.
Other possible sources of the observed low δ56Fe values, such as biomass burning and volcanic emissions, were taken into account. There was an impact from biomass burning in Siberian forest fires during the sampling period of 14-M and 14-N, according to Jung et al. (2016) and Kamezaki et al. (2019). In addition, the fine particles in 14-N yielded a low δ56Fe value. However, our previous study suggested that the δ56Fe of aerosols emitted from biomass burning is not particularly low because of (i) the preferential emission of Fe by soil suspensions with a value of δ56Fe that is close to the crustal average and (ii) the low combustion temperatures (300 to 500 ∘C), which are not high enough for the emission of large amounts of Fe to occur via evaporation (Kurisu and Takahashi, 2019). Although some plants have values of δ56Fe as low as −1.6 ‰ (Guelke and Von Blanckenburg, 2007), they are not considered to be an important Fe source emitted by biomass burning because the Fe content in plants is low compared with that of soil. The low δ56Fe value observed in 14-N may have been a result of the significant influence of combustion Fe originating from coal combustion because a high EFPb was observed (Nriagu and Pacyna, 1988; Zhang et al., 2009). Taken together, these observations suggest that biomass burning cannot explain the low δ56Fe, although Fe from biomass burning may have influenced the results in terms of Fe concentrations.
There are no data concerning the δ56Fe of aerosols emitted by volcanic activity. The typical δ56Fe range of volcanic rocks is −0.3 ‰ to 0.3 ‰ (Fantle and DePaolo, 2004; Heimann et al., 2008), whereas it is possible that volcanic emissions have a low δ56Fe value as a result of isotope fractionation during evaporation, considering that Fe evaporates as gaseous Fe chloride (FeCl2 or FeCl3), based on thermodynamic calculations (Symonds et al., 1992); further studies are required to investigate this. According to the volcanic eruption database (Global Volcanism Program, Smithsonian Institution, https://volcano.si.edu/, last access: 30 May 2021), there were several volcanic activity events around the Aleutian Islands during the sampling periods. However, low δ56Fe values were not observed around this area, suggesting that volcanic emission was not the reason for the low δ56Fe values observed in the present study.
To the best of our knowledge, there are no reported aerosol sources with a low δ56Fe other than anthropogenic combustion Fe. Thus, we conclude that the low δ56Fe values were due to the presence of combustion Fe.
4.1.2 The origin of Fe with δ56Fe values close to or higher than 0 ‰
Most of the coarse particles and some of the fine particles from samples collected over the open ocean yielded δ56Fe values close to 0.0 ‰, which is the typical value of crustal materials (Beard et al., 2003; Johnson et al., 2003). Considering that the major source of Fe is mineral dust, most of the particles can be considered to be of crustal origin.
δ56Fe values as high as 0.45 ‰ were observed in some of the samples, especially those collected over the open ocean. We confirmed that these values were not caused by interference from any other elements during measurements, such as 54Cr on 54Fe or 40Ar23Na on 63Cu. On the whole, high δ56Fe values tended to be observed when the Fe concentration was low (<5 ng m−3, Fig. S8a). Labatut et al. (2014) also reported that δ56Fe values (0.27 ± 0.15 ‰ to 0.38 ± 0.08 ‰) in the western equatorial Pacific were relatively high compared with those of typical mineral aerosols. Possible explanations for these high δ56Fe values are (i) another Fe source with high δ56Fe values or (ii) the long-range transport of lithogenic aerosols along with a change in δ56Fe values.
In the case of (i), several sources can be considered, such as mineral dust with high δ56Fe values and sea spray aerosol (SSA). The δ56Fe values of crustal materials typically lie within the range of −0.3 ‰ to 0.3 ‰ (Fantle and DePaolo, 2004; Johnson et al., 2003; Majestic et al., 2009; Mead et al., 2013), and an average δ56Fe value of 0.09 ± 0.03 ‰ has been reported for the Chinese Loess Plateau (Gong et al., 2017). However, Fe isotope fractionation can occur during continental weathering, the extent of which is determined by the combination of equilibrium and kinetic processes (Cornell and Schwertmann, 2003; Dideriksen et al., 2010; Liu et al., 2014; Wiederhold et al., 2007). If such minerals are selectively transported as aerosols, δ56Fe values that are different from the average dust values may be observed. However, such high δ56Fe values have not been reported in coarse aerosols on land, which contain a larger fraction of mineral dust. Therefore, the reason why only marine aerosols show such high δ56Fe values is unclear. Surface seawater generally has a high δ56Fe of dissolved Fe up to 0.7 ‰ as a result of biological uptake of lighter Fe (Conway and John, 2014; Ellwood et al., 2015; Radic et al., 2011). The concentration of dissolved Fe in the surface seawater of the open ocean in the North Pacific is generally low, typically less than 0.2 nmol L−1 (Nishioka and Obata, 2017), whereas its concentration is approximately 2 orders of magnitude higher in SSA compared with its concentration in the surface seawater, according to Weisel et al. (1984). Although no data are available concerning the δ56Fe of SSA, it is possible that high values of δ56Fe are reflected in SSA. Considering that SSA contains Na as the main component, the molar ratios and δ56Fe values were compared (Fig. S8b). However, no clear trend was obtained, suggesting that the high δ56Fe values cannot be explained by the presence of SSA alone.
In the case of explanation (ii), in which the long-range transport of lithogenic aerosols is accompanied by a change in δ56Fe values, a proportion of each particle with a low δ56Fe value needs to be selectively removed to change the aerosol δ56Fe values during transport. For example, considering the photochemical or acidification process of a single particle, the surface of the particle preferentially reacts with acidic water and becomes more soluble, isotope fractionation occurs between the soluble and insoluble phases, and the soluble and insoluble phases become enriched with lighter and heavier Fe isotopes, respectively (Kiczka et al., 2010; Revels et al., 2015; Wiederhold et al., 2006). However, the selective removal of the soluble phase of the particle is needed to change aerosol δ56Fe values. Although soluble Fe is preferentially incorporated into clouds and removed by precipitation, it is unknown whether the selective removal of the soluble phase in a single particle occurs. In addition, there was no relationship between the δ56Fe value and the average solar radiation flux calculated along the backward trajectory, suggesting that the high δ56Fe values cannot be explained solely by the difference in photochemical activity (Fig. S9a), although we could not discuss the extent of the acidification process. This possibility, therefore, requires further study.
Although it is not easy to obtain any clear conclusions at present, clarifying the reason for the high δ56Fe will lead to a better understanding of the transport processes and sources of Fe. We plan to investigate this in the future, as the current study was focused on whether the low δ56Fe observed is caused by combustion processes.
4.2 Factors controlling fractional Fe solubility
As discussed in Sect. 4.1, low δ56Fe values suggest the presence of combustion Fe. By comparing the δ56Fe values of total (acid-digested) Fe and fractional Fe solubilities, the importance of combustion Fe as a controlling factor to determine fractional Fe solubility can be discussed. A good correlation between the fractional Fe solubility and δ56Fe value of the total Fe was observed in the group I samples (Fig. 8a). Assuming that combustion Fe has a constant δ56Fe value, a lower δ56Fe value corresponds to a larger fraction of combustion Fe in a sample. The fact that the soluble fraction in the fine particles of group I yielded δ56Fe values lower than the total (acid-digested) Fe (Table S5) indicated that combustion Fe with a low δ56Fe value was preferentially extracted.
Previous studies have suggested that combustion Fe is more soluble than natural Fe because it is present mainly as an amorphous glass or aggregates of iron (hydr)oxide nanoparticles, which have higher solubilities and dissolution rates than the natural Fe that is usually found in aluminosilicate structures (Chen et al., 2012; Ito and Shi, 2016). Furthermore, combustion Fe is often emitted along with other acids, such as sulfates, leading to greater aerosol acidity and thus larger fractional Fe solubility (Buck et al., 2006; Ingall et al., 2018; Li et al., 2017). Our results indicated a weak correlation between the fraction of (hydr)oxides and the δ56Fe value (Fig. 8c) and between the fraction of (hydr)oxides and the fractional Fe solubility in the group I samples, although there were insufficient data concerning the latter (n=4, Fig. 8e). These results indicated that combustion Fe contained a large fraction of (hydr)oxides, which was partially responsible for the high fractional Fe solubilities. Therefore, the presence of combustion Fe was an important factor in controlling the fractional solubility in the area from which the group I samples were taken.
The fractional Fe solubilities of the group II and III samples were not correlated with δ56Fe (Fig. 8b); although their δ56Fe values were close to or higher than 0 ‰, their fractional Fe solubilities varied from 0.1 % to 23 %. Therefore, factors other than the effect of combustion Fe may be more important for controlling the fractional Fe solubility in the open ocean. Although some of the fine particles showed higher fractional Fe solubilities when the fraction of (hydr)oxides was high, this was not the case for the other samples (Fig. 8d), suggesting that the presence of (hydr)oxides cannot fully explain the variation in the fractional Fe solubilities. A high solar radiation flux enhances photochemical reduction of Fe(III), especially under the presence of organic ligands, which can change fractional Fe solubilities and Fe species (Chen and Grassian, 2013; Pehkonen et al., 1993). Because KH-13-7 and KH-14-3 samples were collected during winter and summer, respectively, their solar radiation fluxes were substantially different (Tables S1 and S2). However, we did not find any effects of solar radiation fluxes on fractional Fe solubilities and Fe species between the winter (KH-13-7) and the summer (KH-14-3) samples (Fig. S9b and c). One possibility is the presence of other Fe species with high fractional Fe solubilities that could not be detected by XAFS analysis (due to smaller fractions of <10 %). For example, Fe sulfate has a high fractional Fe solubility, which was only found by µ-XAFS analysis (Fig. S5). In addition, other factors, such as in situ aerosol acidity or the presence of Fe-binding organic ligands (e.g., oxalate), may be important for Fe dissolution following long-range atmospheric transport (Chen and Grassian, 2013; Ito and Shi, 2016).
As noted in Sect. 3.2, high fractional solubilities were obtained when Fe concentrations were low (Fig. S3). This trend is considered to be caused by (i) the longer lifetime of fine particles that contain large amounts of combustion Fe with high fractional solubility and/or (ii) an increase in the fractional Fe solubility during atmospheric transport (Mahowald et al., 2018). From a scatter plot showing the atmospheric Fe concentration and fractional Fe solubility in which the color scale shows the difference in the values of δ56Fe (Fig. S10), the importance of the presence of combustion Fe can be investigated. A high fractional Fe solubility was not obtained only when the δ56Fe was low, again suggesting that a combination of several factors controls fractional Fe solubility. The processes that influence fractional Fe solubility could be investigated using the Fe isotope ratio as another parameter.
4.3 The contribution of combustion Fe to marine aerosols
We estimated the relative contribution of combustion Fe based on the mass balance equation for coarse (>2.5 µm) and fine (<2.5 µm) particles using the following equations:
where fcombustion-fine and fcombustion-coarse are the fractions of combustion Fe in fine and coarse particles, respectively. The representative δ56Fe value of combustion Fe was estimated to be −3.9 ‰ to −4.7 ‰ based on the δ56Fe values of the aerosol samples collected at various sites, which included suburban areas and sites near sources of anthropogenic emissions (Kurisu et al., 2016a, 2016b, 2019; Kurisu and Takahashi, 2019). The δ56Fe value of natural Fe was assumed to be the same as the crustal average of 0.0 ‰ (Beard et al., 2003). We assumed that samples were of natural origin even when they exhibited values of δ56Fe higher than 0.0 ‰ based on the discussion in Sect. 4.1. Although the evaluation of samples 14-N and 14-O has been already discussed in Kurisu et al. (2016b, 2019), in the present study these results were combined with the data describing the other 18 samples.
The calculated fractions of combustion Fe in fine and coarse particles were up to 50 % and 6 %, respectively, near the Japanese coast and up to 21 % when calculating the fraction for the bulk (fine + coarse) particles. These results suggest the importance of combustion Fe even in marine aerosols (Fig. 9, Table 1). The fractions in the group I samples were higher in the summer (KH-14-3, on average 20 %) than in the winter (KH-13-7, on average 6 %), which suggests that the influence of mineral dust from East Asia was greater during the winter (KH-13-7) than the summer (KH-14-3). However, the influence of combustion Fe was only seen in group I (approximately 2000–3000 km from East Asia) and was not observed in the group II and III regions. Natural Fe was more important when air masses were from the eastern, central, or northern Pacific.
The fraction of combustion Fe to soluble Fe was also calculated from the δ56Fe of the soluble component in sample 13-e (−1.14 ± 0.03 ‰, Table S5). We assumed that the δ56Fe of the soluble component of combustion Fe is the same as the total fraction (−3.9 ‰ to −4.7 ‰) and that the δ56Fe of the soluble component of natural Fe is the same as that of the coarse particles in 13-e (−0.27 ± 0.03 ‰, Table S5) considering that kinetic isotope fractionation of natural Fe also occurred in the fine particles, as discussed in Sect. 3.4. The ratio of combustion Fe in the soluble Fe of fine particles was approximately 22 ± 2 %, which was higher than that of the total (soluble + insoluble) Fe (11 ± 4 %, Table 1). From these results, the fractional Fe solubilities of natural and combustion Fe could also be calculated according to the following equation:
where SFefine and TFefine are the soluble and total (acid-digested) Fe concentrations, respectively, and fsol-comb-fine and ftotal-comb-fine are the fractions of combustion Fe in the soluble and total fractions, respectively, estimated by Eq. (6). The same calculation was conducted for natural Fe. The calculated fractional Fe solubilities were 0.9 % and 11 % for natural and combustion Fe, respectively. The higher fractional Fe solubility of combustion Fe than natural Fe again suggests the importance of combustion Fe as a source of soluble Fe, even though the emissions of combustion Fe are much smaller than natural Fe emissions.
4.4 Comparison with a model estimation
The contributions of combustion Fe to the total (soluble + insoluble) Fe in the marine aerosols estimated by the IMPACT model during the sampling periods were compared with those estimated by the Fe isotope ratios (Table 1).
The contributions from combustion Fe estimated by the Fe isotope ratios and the IMPACT model were similar in fine particles of groups I and II (Table 1). The high proportions of combustion Fe in the fine particles in group I were reproduced mainly by Comp 3 (anthropogenic combustion on land, mainly from coal combustion and the steel industry) in the IMPACT model, whereas there were smaller contributions from oil combustion. The low contributions of combustion Fe in group II were also reproduced by the IMPACT model. Although only the δ56Fe of fine particles of sample 14-L could be analyzed in group III, the IMPACT model estimated relatively large contributions from combustion Fe (mainly oil combustion) in group III, which was not suggested by the Fe isotope ratio. It is possible that (i) the IMPACT model overestimated the contribution of Fe from oil combustion in remote oceans or (ii) the δ56Fe value of combustion Fe estimated at −3.9 ‰ to −4.7 ‰ could not be applied to the estimation of the contribution of oil combustion. Because most Fe in liquid fuels might be released into the atmosphere (e.g., 93 % according to Wang et al., 2003), there might be limited Fe isotope fractionation during oil combustion. As there are no data concerning the δ56Fe of atmospheric aerosols emitted by the combustion of oil, further studies regarding the δ56Fe value of a more specific source are required.
The combustion Fe fractions in coarse particles estimated by the model were often higher than the isotope-based estimates, especially near the Japanese coast (Table 1). A possible reason for this difference is the various characteristics of the “combustion Fe” that are included in the calculation. Combustion Fe estimated by the Fe isotope ratios is limited to Fe with low values of δ56Fe, which is emitted by evaporation under high-temperature conditions. Such evaporated Fe comprises aggregates of Fe (hydr)oxide particles mainly contained in fine-sized particle fractions (Kurisu et al., 2016a, b, 2019). In contrast, the model estimates emissions from anthropogenic combustion sources based on the emission inventory dataset produced by the Community Emission Data System (Hoesly et al., 2018) and the Fe fraction for each particle size and from each emission source (Ito et al., 2018). Therefore, combustion Fe in the model-based estimation includes Fe emitted not only by evaporation processes but also by other processes, such as melting and fragmentation in coal combustion (Rathod et al., 2020), especially in coarse particles. Actually, coarse particles with relatively high EFFe values and δ56Fe close to 0 ‰ observed near the Japanese coast suggest the presence of anthropogenic Fe, which was not emitted by evaporation. This could have led to a larger contribution from combustion Fe to the coarse particles near emission sources. Considering that the low δ56Fe corresponds to high fractional Fe solubility, it is suggested that evaporated Fe has high fractional Fe solubility and that the δ56Fe is important to estimate the contribution of combustion Fe with high fractional solubility, although not all combustion Fe estimated by the model is included.
These results also indicate the importance of using δ56Fe data on size-fractionated aerosols to evaluate the combustion Fe emission estimated by the model. To explain this, the δ56Fe values were reproduced according to Eq. (6) using the fcombustion estimated by the IMPACT model and were compared with the observational results (Fig. 10). When the δ56Fe values were reproduced for the bulk (coarse + fine) particles based on the results of the IMPACT model, they were much lower than the observed δ56Fe values, especially in group I samples. However, when calculating the values for fine particles only, they were better reproduced. Thus, the reduction in the combustion Fe emissions to fit the observed higher bulk δ56Fe could mislead the model into underestimating the contribution of combustion Fe.
It should also be noted that the calculation of the fractions of combustion Fe largely depends on the δ56Fe of combustion Fe. Conway et al. (2019) conducted a similar comparison by applying −1.6 ‰ as the δ56Fe of combustion Fe, which is higher than that used in this study. They estimated 50 % to 100 % of the contribution of combustion Fe to soluble Fe in European and North American aerosols and suggested the underestimation of combustion Fe in a model calculation. As studies on the δ56Fe of combustion Fe are limited, further studies into the δ56Fe of combustion Fe from various sources and in different regions will lead to a more quantitative understanding of the fraction of combustion Fe, which in turn will contribute to a more accurate prediction of the distribution of natural and combustion Fe in aerosols.
To further clarify the reasons for the difference between the observed and model results, the Fe concentration of each source was compared with that estimated by the model. Although the bulk (fine + coarse) Fe concentrations were reproduced well by the model, the model underestimated the coarse Fe concentrations and overestimated the fine Fe concentrations compared with those from observations (Fig. S11). This is partly because of the different size distribution of mineral dust from observations and the IMPACT model (Fig. S11a and b); the IMPACT model tended to underestimate the contribution of coarse mineral dust, as previously suggested by Adebiyi and Kok (2020) and Ito et al. (2021b). The extent of overestimation and underestimation was larger when the Fe concentrations were low. Observational data on Fe concentrations and δ56Fe for size-fractionated aerosols in the open ocean will help improve the accuracy of the model estimation.
4.5 Contribution of atmospheric Fe deposition to the surface seawater
Our results suggest that Fe from anthropogenic combustion is an important source of soluble Fe in air masses from the direction of East Asia. The dry deposition fluxes (F) of total and soluble Fe from combustion and natural Fe were roughly estimated for each group according to the following equation:
where C is the atmospheric Fe concentrations, in which the average total and soluble Fe concentrations in each group were used for the calculation. V is the deposition rate of coarse and fine particles, which was assumed to be 1000 and 260 m d−1, respectively, although these values can change depending on the wind speed and humidity (Buck et al., 2019; Duce and Tindale, 1991). To calculate the soluble Fe concentrations of the combustion and natural Fe in group I, the fractional Fe solubilities of combustion and natural Fe were estimated to be 11 % and 0.9 %, respectively, based on the values calculated from sample 13-e in Sect. 4.3.
The deposition fluxes of total Fe in group I were approximately 201 and 15 nmol m−2 d−1 for the natural and combustion sources, respectively (Table S8, Fig. 11), while those of soluble Fe were 2.9 and 1.4 nmol m−2 d−1, respectively. Group I received a large contribution of combustion Fe (33 %) to the soluble Fe flux, suggesting the importance of combustion Fe as a source of soluble Fe in surface seawater despite its lower emission than natural sources. When considering the contribution of soluble Fe to the surface ocean, combustion and natural aerosol deposition could be important compared with other Fe sources, which are mainly transported from deeper layers of seawater, although this largely depends on the area and the season with a wide range of Fe flux from 0.5 to 20 nmol m−2 d−1 (Nishioka et al., 2007, 2020). Although there were no observational data for wet deposition in the present study, wet deposition flux has been shown to be larger than dry deposition flux in the western North Pacific (Uematsu et al., 1985). The IMPACT model also estimated the soluble Fe flux by dry and wet depositions during the group I sampling period, in which dry deposition accounted for up to 20 % of the total deposition flux (Fig. S12), indicating a much larger bulk (wet + dry) deposition flux of soluble Fe than the dry deposition only. If the contribution of combustion Fe to surface seawater is substantial, the low δ56Fe could be reflected in the surface seawater (Pinedo-González et al., 2020). Simultaneous sampling and Fe isotope analysis of aerosols and surface seawater should allow the direct investigation of the importance of Fe in aerosols to the budget of soluble and insoluble Fe in the surface seawater.
The Fe deposition fluxes in groups II (27 and 0.2 nmol m−2 d−1 for total and soluble Fe, respectively) and III (32 and 0.4 nmol m−2 d−1 for total and soluble Fe, respectively) were only from natural sources. They were lower than those in group I by an order of magnitude (Table S8) and also considerably lower than those observed in previous studies (Buck et al., 2019; Duce and Tindale, 1991; Uematsu et al., 1983, 1985). Previous studies have reported the long-range transport of a large quantity of mineral dust to the central North Pacific during spring (e.g., Buck et al., 2006; Uematsu et al., 1983). Therefore, if air masses are transported from the direction of East Asia, it is possible that the larger influence of atmospheric Fe, including combustion Fe, could occur more widely and also contribute to the increase in the supply of Fe to HNLC regions.
Size-fractionated aerosol samples were collected in the northwestern Pacific to estimate the relative contribution of anthropogenic combustion Fe and natural Fe to marine aerosols and to investigate the factors that control fractional Fe solubility. Air masses from the direction of East Asia included fine particles that yielded δ56Fe values 0.5 ‰ to 2 ‰ lower than those of the coarse particles because of the presence of combustion Fe. The δ56Fe values of coarse and fine particles in air masses from the eastern, central, or northern Pacific were close to the crustal value. It was also found that in air masses from the direction of East Asia, fractional Fe solubilities are mainly controlled by the presence of combustion Fe. The proportion of combustion Fe in the total Fe in marine aerosols was up to 51 % and 20 % in fine and bulk (fine + coarse) particles, respectively. In addition, the contribution of combustion Fe was greater in the soluble component, suggesting the importance of combustion Fe as a source of Fe in the surface ocean. However, the influence of combustion Fe was limited in the vicinity of East Asia, and natural Fe was the main source of aerosol Fe in air masses from the eastern, central, or northern Pacific. The comparison of the contribution of combustion Fe estimated by the IMPACT model with that estimated by the Fe isotope ratio suggested that δ56Fe values of size-fractionated aerosol are important to make this comparison due to the different characteristics of “combustion Fe” included in the different approaches, in which combustion Fe estimated using Fe isotope ratios is limited to particles emitted by evaporation mainly contained in fine particles. Considering that the δ56Fe values were correlated with fractional Fe solubilities, isotope-based estimation is important when discussing the contribution of combustion Fe with high fractional Fe solubility. Although the influence of combustion Fe was limited adjacent to the Japanese coast in terms of samples in this study with relatively lower concentrations of Fe, the contribution may be much larger when air masses are transported to the open ocean from East Asia, such as during springtime in the Northern Hemisphere. This study showed the applicability of Fe isotope data to further understanding atmospheric Fe sources and their fractional Fe solubilities. The large contribution of combustion Fe to the marine atmosphere also suggests the possible contribution of combustion Fe to the surface seawater. Iron isotope data will help clarify the contribution of combustion Fe to seawater; it is anticipated that this will lead to a more quantitative understanding of Fe cycling in the atmosphere–surface ocean system.
More detailed data are available upon request (Minako Kurisu, email@example.com).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-21-16027-2021-supplement.
MK and YT designed the research. MU established the sampling methods and collected aerosol samples during the cruises. MK, KS, and YT conducted sample analysis. AI developed the model code and performed the simulations. MK prepared the paper with contributions from all co-authors.
The contact author has declared that neither they nor their co-authors have any competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We appreciate Tsuyoshi Iizuka for technical support with the isotope analysis. XAFS analysis was conducted with the approval of KEK-PF (2016G632, 2018G575, 2018G089, 2019G093).
This research has been supported by the Japan Society for the Promotion of Science (grant nos. 17J06716, 18H04134, and 20H04329) and the Integrated Research Program for Advancing Climate Models (TOUGOU) from the Ministry of Education, Culture, Sports, Science and Technology (grant no. JPMXD0717935715).
This paper was edited by Jerome Brioude and reviewed by two anonymous referees.
Adebiyi, A. A. and Kok, J. F.: Climate models miss most of the coarse dust in the atmosphere, Sci. Adv., 6, 1–10, https://doi.org/10.1126/sciadv.aaz9507, 2020.
Albarede, F., Telouk, P., Blichert-Toft, J., Boyet, M., Agranier, A., Nelson, B., Albarède, F., Telouk, P., Blichert-Toft, J., Boyet, M., Agranier, A., and Nelson, B.: Precise and accurate isotopic measurements using multiple-collector ICPMS, Geochim. Cosmochim. Ac., 68, 2725–2744, https://doi.org/10.1016/j.gca.2003.11.024, 2004.
Baker, A. R. and Jickells, T. D.: Mineral particle size as a control on aerosol iron solubility, Geophys. Res. Lett., 33, 1–4, https://doi.org/10.1029/2006GL026557, 2006.
Beard, B. L., Johnson, C. M., Skulan, J. L., Nealson, K. H., Cox, L., and Sun, H.: Application of Fe isotopes to tracing the geochemical and biological cycling of Fe, Chem. Geol., 195, 87–117, https://doi.org/10.1016/S0009-2541(02)00390-X, 2003.
Berry, A. J., O'Neill, H. S. C., Jayasuriya, K. D., Campbell, S. J., and Foran, G. J.: XANES calibrations for the oxidation state of iron in a silicate glass, Am. Mineral., 88, 967–977, https://doi.org/10.2138/am-2003-0704, 2003.
Buck, C. S., Landing, W. M., Resing, J. A., and Lebon, G. T.: Aerosol iron and aluminum solubility in the northwest Pacific Ocean: Results from the 2002 IOC cruise, Geochem. Geophy. Geosy., 7, 1–21, https://doi.org/10.1029/2005GC000977, 2006.
Buck, C. S., Aguilar-Islas, A., Marsay, C., Kadko, D., and Landing, W. M.: Trace element concentrations, elemental ratios, and enrichment factors observed in aerosol samples collected during the US GEOTRACES eastern Pacific Ocean transect (GP16), Chem. Geol., 511, 212–224, https://doi.org/10.1016/j.chemgeo.2019.01.002, 2019.
Charlson, R. J., Lovecook, J. E., Andreae, M. O., and Warren, S. G.: Ocean phytoplankton, atmospheric sulfur, cloud albdeo and climate, Nature, 326, 655–661, https://doi.org/10.1029/2003GB002183, 1987.
Chen, H. and Grassian, V. H.: Iron dissolution of dust source materials during simulated acidic processing: The effect of sulfuric, acetic, and oxalic acids, Environ. Sci. Technol., 47, 10312–10321, https://doi.org/10.1021/es401285s, 2013.
Chen, H., Laskin, A., Baltrusaitis, J., Gorski, C. A., Scherer, M. M., and Grassian, V. H.: Coal fly ash as a source of iron in atmospheric dust, Environ. Sci. Technol., 46, 2112–2120, https://doi.org/10.1021/es204102f, 2012.
Ciais, P., Sabine, C., Bala, G., Bopp, L., Brovkin, V., Canadell, J., Chhabra, A., DeFries, R., Galloway, J., Heimann, M., Jones, C., Quéré, C. Le, Myneni, R. B., Piao, S., and Thornton, P.: “Carbon and other biogeochemical cycles”, Climate change 2013: the physical science basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change, Cambridge University Press, Cambridge University Press, Cambridge, UK and New York, NY, USA, 2014.
Conway, T. M. and John, S. G.: Quantification of dissolved iron sources to the North Atlantic Ocean, Nature, 511, 212–215, https://doi.org/10.1038/nature13482, 2014.
Conway, T. M., Rosenberg, A. D., Adkins, J. F., and John, S. G.: A new method for precise determination of iron, zinc and cadmium stable isotope ratios in seawater by double-spike mass spectrometry, Anal. Chim. Acta, 793, 44–52, https://doi.org/10.1016/j.aca.2013.07.025, 2013.
Conway, T. M., Hamilton, D. S., Shelley, R. U., Aguilar-Islas, A. M., Landing, W. M., Mahowald, N. M., and John, S. G.: Tracing and constraining anthropogenic aerosol iron fluxes to the North Atlantic Ocean using iron isotopes, Nat. Commun., 10, 1–10, https://doi.org/10.1038/s41467-019-10457-w, 2019.
Cornell, R. M. and Schwertmann, U.: The iron oxides, structure, properties, reactions, occurrences and uses, 2nd Edn., Wiley-VCH Pub., Weinheim, Germany, 2003.
Dauphas, N., John, S. G., and Rouxel, O.: Iron isotope systematics, Rev. Mineral. Geochem., 82, 415–510, https://doi.org/10.2138/rmg.2017.82.11, 2017.
Dideriksen, K., Christiansen, B. C., Frandsen, C., Balic-Zunic, T., Mørup, S., and Stipp, S. L. S.: Paleo-redox boundaries in fractured granite, Geochim. Cosmochim. Ac., 74, 2866–2880, https://doi.org/10.1016/j.gca.2010.02.022, 2010.
Duce, R. A. and Tindale, N. W.: Atmospheric transport of iron and its deposition in the ocean, Limnol. Oceanogr., 36, 1715–1726, https://doi.org/10.4319/lo.1918.104.22.1685, 1991.
Duce, R. A., Liss, P. S., Merrill, J. T., Atlas, E. L., Buat-Menard, P., Hicks, B. B., Miller, J. M., Prospero, J. M., Arimoto, R., Church, T. M., Ellis, W., Galloway, J. N., Hansen, L., Jickells, T. D., Knap, A. H., Reinhardt, K. H., Schneider, B., Soudine, A., Tokos, J. J., Tsunogai, S., Wollast, R., and Zhou, M.: The atmospheric input of trace species to the world ocean, Global Biogeochem. Cy., 5, 193–259, https://doi.org/10.1029/91GB01778, 1991.
Ellwood, M. J., Hutchins, D. A., Lohan, M. C., Milne, A., Nasemann, P., Nodder, S. D., Sander, S. G., Strzepek, R., Wilhelm, S. W., and Boyd, P. W.: Iron stable isotopes track pelagic iron cycling during a subtropical phytoplankton bloom, Proc. Natl. Acad. Sci., 112, 15–20, https://doi.org/10.1073/pnas.1421576112, 2015.
Falkowski, P. G., Barber, R. T., and Smetacek, V.: Biogeochemical controls and feedbacks on ocean primary production, Science, 281, 200–206, https://doi.org/10.1126/science.281.5374.200, 1998.
Fantle, M. S. and DePaolo, D. J.: Iron isotopic fractionation during continental weathering, Earth Planet. Sc. Lett., 228, 547–562, https://doi.org/10.1016/j.epsl.2004.10.013, 2004.
Fitzsimmons, J. N., John, S. G., Marsay, C. M., Hoffman, C. L., Nicholas, S. L., Toner, B. M., German, C. R., and Sherrell, R. M.: Iron persistence in a distal hydrothermal plume supported by dissolved-particulate exchange, Nat. Geosci., 10, 195–201, https://doi.org/10.1038/ngeo2900, 2017.
Gong, Y., Xia, Y., Huang, F., and Yu, H.: Average iron isotopic compositions of the upper continental crust: constrained by loess from the Chinese Loess Plateau, Acta Geochim., 36, 125–131, https://doi.org/10.1007/s11631-016-0131-5, 2017.
Guelke, M. and Von Blanckenburg, F.: Fractionation of stable iron isotopes in higher plants, Environ. Sci. Technol., 41, 1896–1901, https://doi.org/10.1021/es062288j, 2007.
Hamilton, D. S., Moore, J. K., Arneth, A., Bond, T. C., Carslaw, K. S., Hantson, S., Ito, A., Kaplan, J. O., Lindsay, K., Nieradzik, L., Rathod, S. D., Scanza, R. A., and Mahowald, N. M.: Impact of Changes to the Atmospheric Soluble Iron Deposition Flux on Ocean Biogeochemical Cycles in the Anthropocene, Global Biogeochem. Cy., 34, 1–22, https://doi.org/10.1029/2019GB006448, 2020.
Heimann, A., Beard, B. L., and Johnson, C. M.: The role of volatile exsolution and sub-solidus fluid/rock interactions in producing high 56Fe 54Fe ratios in siliceous igneous rocks, Geochim. Cosmochim. Ac., 72, 4379–4396, https://doi.org/10.1016/j.gca.2008.06.009, 2008.
Hoesly, R. M., Smith, S. J., Feng, L., Klimont, Z., Janssens-Maenhout, G., Pitkanen, T., Seibert, J. J., Vu, L., Andres, R. J., Bolt, R. M., Bond, T. C., Dawidowski, L., Kholod, N., Kurokawa, J. I., Li, M., Liu, L., Lu, Z., Moura, M. C. P., O'Rourke, P. R., and Zhang, Q.: Historical (1750–2014) anthropogenic emissions of reactive gases and aerosols from the Community Emissions Data System (CEDS), Geosci. Model Dev., 11, 369–408, https://doi.org/10.5194/gmd-11-369-2018, 2018.
Ingall, E., Feng, Y., Longo, A., Lai, B., Shelley, R., Landing, W., Morton, P., Nenes, A., Mihalopoulos, N., Violaki, K., Gao, Y., Sahai, S., and Castorina, E.: Enhanced Iron Solubility at Low pH in Global Aerosols, Atmosphere (Basel), 9, 1–17, https://doi.org/10.3390/atmos9050201, 2018.
Ito, A.: Atmospheric processing of combustion aerosols as a source of bioavailable iron, Environ. Sci. Technol. Lett., 2, 70–75, https://doi.org/10.1021/acs.estlett.5b00007, 2015.
Ito, A. and Shi, Z.: Delivery of anthropogenic bioavailable iron from mineral dust and combustion aerosols to the ocean, Atmos. Chem. Phys., 16, 85–99, https://doi.org/10.5194/acp-16-85-2016, 2016.
Ito, A., Lin, G., and Penner, J. E.: Radiative forcing by light-absorbing aerosols of pyrogenetic iron oxides, Sci. Rep., 8, 1–11, https://doi.org/10.1038/s41598-018-25756-3, 2018.
Ito, A., Myriokefalitakis, S., Kanakidou, M., Mahowald, N. M., Scanza, R. A., Hamilton, D. S., Baker, A. R., Jickells, T., Sarin, M., Bikkina, S., Gao, Y., Shelley, R. U., Buck, C. S., Landing, W. M., Bowie, A. R., Perron, M. M. G., Guieu, C., Meskhidze, N., Johnson, M. S., Feng, Y., Kok, J. F., Nenes, A., and Duce, R. A.: Pyrogenic iron: The missing link to high iron solubility in aerosols, Sci. Adv., 5, 13–15, https://doi.org/10.1126/sciadv.aau7671, 2019.
Ito, A., Ye, Y., Yamamoto, A., Watanabe, M., and Aita, M. N.: Responses of ocean biogeochemistry to atmospheric supply of lithogenic and pyrogenic iron-containing aerosols, Geol. Mag., 157, 741–756, https://doi.org/10.1017/S0016756819001080, 2020.
Ito, A., Ye, Y., Baldo, C., and Shi, Z.: Ocean fertilization by pyrogenic aerosol iron, npj Clim. Atmos. Sci., 4, 30, https://doi.org/10.1038/s41612-021-00185-8, 2021a.
Ito, A., Adebiyi, A. A., Huang, Y., and Kok, J. F.: Less atmospheric radiative heating due to aspherical dust with coarser size, Atmos. Chem. Phys. Discuss. [preprint], https://doi.org/10.5194/acp-2021-134, in review, 2021b.
Jickells, T. D.: Global iron connections between desert dust, ocean biogeochemistry, and climate, Science, 308, 67–71, https://doi.org/10.1126/science.1105959, 2005.
John, S. G. and Adkins, J. F.: Analysis of dissolved iron isotopes in seawater, Mar. Chem., 119, 65–76, https://doi.org/10.1016/j.marchem.2010.01.001, 2010.
Johnson, C. M., Beard, B. L., Beukes, N. J., Klein, C., and O'Leary, J. M.: Ancient geochemical cycling in the Earth as inferred from Fe isotope studies of banded iron formations from the Transvaal Craton, Contrib. Mineral. Petrol., 144, 523–547, https://doi.org/10.1007/s00410-002-0418-x, 2003.
Jung, J., Lyu, Y., Lee, M., Hwang, T., Lee, S., and Oh, S.: Impact of Siberian forest fires on the atmosphere over the Korean Peninsula during summer 2014, Atmos. Chem. Phys., 16, 6757–6770, https://doi.org/10.5194/acp-16-6757-2016, 2016.
Kamezaki, K., Hattori, S., Iwamoto, Y., Ishino, S., Furutani, H., Miki, Y., Uematsu, M., Miura, K., and Yoshida, N.: Tracing the sources and formation pathways of atmospheric particulate nitrate over the Pacific Ocean using stable isotopes, Atmos. Environ., 209, 152–166, https://doi.org/10.1016/j.atmosenv.2019.04.026, 2019.
Kiczka, M., Wiederhold, J. G., Frommer, J., Kraemer, S. M., Bourdon, B., and Kretzschmar, R.: Iron isotope fractionation during proton- and ligand-promoted dissolution of primary phyllosilicates, Geochim. Cosmochim. Ac., 74, 3112–3128, https://doi.org/10.1016/j.gca.2010.02.018, 2010.
Kodama, S., Takahashi, Y., Okumura, K., and Uruga, T.: Speciation of iodine in solid environmental samples by iodine K-edge XANES: Application to soils and ferromanganese oxides, Sci. Total Environ., 363, 275–284, https://doi.org/10.1016/j.scitotenv.2006.01.004, 2006.
Kurisu, M. and Takahashi, Y.: Testing iron stable isotope ratios as a signature of biomass burning, Atmosphere (Basel), 10, 1–15, https://doi.org/10.3390/atmos10020076, 2019.
Kurisu, M., Sakata, K., Miyamoto, C., Takaku, Y., Iizuka, T., and Takahashi, Y.: Variation of iron isotope ratios in anthropogenic materials emitted through combustion processes, Chem. Lett., 45, 970–972, https://doi.org/10.1246/cl.160451, 2016a.
Kurisu, M., Takahashi, Y., Iizuka, T., and Uematsu, M.: Very low isotope ratio of iron in fine aerosols related to its contribution to the surface ocean, J. Geophys. Res.-Atmos., 121, 11119–11136, https://doi.org/10.1002/2016JD024957, 2016b.
Kurisu, M., Adachi, K., Sakata, K., and Takahashi, Y.: Stable Isotope Ratios of Combustion Iron Produced by Evaporation in a Steel Plant, ACS Earth Sp. Chem., 3, 588–598, https://doi.org/10.1021/acsearthspacechem.8b00171, 2019.
Labatut, M., Lacan, F., Pradoux, C., Chemeleff, J., Radic, A., Murray, J. W., Poitrasson, F., Johansen, A. M., and Thil, F.: Iron sources and dissolved-particulate interactions in the seawater of the Western Equatorial Pacific, iron isotope perspectives, Global Biogeochem. Cy., 28, 1044–1065, https://doi.org/10.1002/2014GB004928, 2014.
Lam, P. J. and Bishop, J. K. B.: The continental margin is a key source of iron to the HNLC North Pacific Ocean, Geophys. Res. Lett., 35, 1–5, https://doi.org/10.1029/2008GL033294, 2008.
Li, W., Xu, L., Liu, X., Zhang, J., Lin, Y., Yao, X., Gao, H., Zhang, D., Chen, J., Wang, W., Harrison, R. M., Zhang, X., Shao, L., Fu, P., Nenes, A., and Shi, Z.: Air pollution–aerosol interactions produce more bioavailable iron for ocean ecosystems, Sci. Adv., 3, 1–7, https://doi.org/10.1126/sciadv.1601749, 2017.
Liu, S. A., Teng, F. Z., Li, S., Wei, G. J., Ma, J. L., and Li, D.: Copper and iron isotope fractionation during weathering and pedogenesis: Insights from saprolite profiles, Geochim. Cosmochim. Ac., 146, 59–75, https://doi.org/10.1016/j.gca.2014.09.040, 2014.
Luo, C., Mahowald, N., Bond, T., Chuang, P. Y., Artaxo, P., Siefert, R., Chen, Y., and Schauer, J.: Combustion iron distribution and deposition, Global Biogeochem. Cy., 22, 1–17, https://doi.org/10.1029/2007GB002964, 2008.
Maggi, V., Baccolo, G., Cibin, G., Delmonte, B., Hampai, D., and Marcelli, A.: XANES Iron Geochemistry in the Mineral Dust of the Talos Dome Ice Core (Antarctica) and the Southern Hemisphere Potential Source Areas, Condens. Matter, 3, 1–15, https://doi.org/10.3390/condmat3040045, 2018.
Mahowald, N. M., Hamilton, D. S., Mackey, K. R. M., Moore, J. K., Baker, A. R., Scanza, R. A., and Zhang, Y.: Aerosol trace metal leaching and impacts on marine microorganisms, Nat. Commun., 9, 1–15, https://doi.org/10.1038/s41467-018-04970-7, 2018.
Majestic, B. J., Anbar, A. D., and Herckes, P.: Elemental and iron isotopic composition of aerosols collected in a parking structure, Sci. Total Environ., 407, 5104–5109, https://doi.org/10.1016/j.scitotenv.2009.05.053, 2009.
Martin, J. H. and Fitzwater, S. E.: Iron de?ciency limits phytoplankton growth in the north-east Paci?c subarctic, Nature, 331, 947–975, https://doi.org/10.1038/331341a0, 1988.
Martin, J. H., Gordon, R. M., Fitzwater, S., and Broenkow, W. W.: Vertex: phytoplankton/iron studies in the Gulf of Alaska, Deep-Sea Res. Pt. A, 36, 649–680, https://doi.org/10.1016/0198-0149(89)90144-1, 1989.
Martin, J. H., Coale, K. H., Johnson, K. S., Fitzwater, S. E., Gordon, R. M., Tanner, S. J., Hunter, C. N., Elrod, V. A., Nowicki, J. L., Coley, T. L., Barber, R. T., Lindley, S., Watson, A. J., Van Scoy, K., Law, C. S., Liddicoat, M. I., Ling, R., Stanton, T., Stockel, J., Collins, C., Anderson, A., Bidigare, R., Ondrusek, M., Latasa, M., Millero, F. J., Lee, K., Yao, W., Zhang, J. Z., Friederich, G., Sakamoto, C., Chavez, F., Buck, K., Kolber, Z., Greene, R., Falkowski, P., Chisholm, S. W., Hoge, F., Swift, R., Yungel, J., Turner, S., Nightingale, P., Hatton, A., Liss, P., and Tindale, N. W.: Testing the iron hypothesis in ecosystems of the equatorial Pacific Ocean, Nature, 371, 123–129, https://doi.org/10.1038/371123a0, 1994.
Matsui, H., Mahowald, N. M., Moteki, N., Hamilton, D. S., Ohata, S., Yoshida, A., Koike, M., Scanza, R. A., and Flanner, M. G.: Anthropogenic combustion iron as a complex climate forcer, Nat. Commun., 9, 1593, https://doi.org/10.1038/s41467-018-03997-0, 2018.
Mead, C., Herckes, P., Majestic, B. J., and Anbar, A. D.: Source apportionment of aerosol iron in the marine environment using iron isotope analysis, Geophys. Res. Lett., 40, 5722–5727, https://doi.org/10.1002/2013GL057713, 2013.
Meskhidze, N., Völker, C., Al-Abadleh, H. A., Barbeau, K., Bressac, M., Buck, C., Bundy, R. M., Croot, P., Feng, Y., Ito, A., Johansen, A. M., Landing, W. M., Mao, J., Myriokefalitakis, S., Ohnemus, D., Pasquier, B., and Ye, Y.: Perspective on identifying and characterizing the processes controlling iron speciation and residence time at the atmosphere-ocean interface, Mar. Chem., 217, 103704, https://doi.org/10.1016/j.marchem.2019.103704, 2019.
Moore, C. M., Mills, M. M., Arrigo, K. R., Berman-Frank, I., Bopp, L., Boyd, P. W., Galbraith, E. D., Geider, R. J., Guieu, C., Jaccard, S. L., Jickells, T. D., La Roche, J., Lenton, T. M., Mahowald, N. M., Marañón, E., Marinov, I., Moore, J. K., Nakatsuka, T., Oschlies, A., Saito, M. A., Thingstad, T. F., Tsuda, A., and Ulloa, O.: Processes and patterns of oceanic nutrient limitation, Nat. Geosci., 6, 701–710, https://doi.org/10.1038/ngeo1765, 2013.
Morton, P. L., Landing, W. M., Hsu, S. C., Milne, A., Aguilar-Islas, A. M., Baker, A. R., Bowie, A. R., Buck, C. S., Gao, Y., Gichuki, S., Hastings, M. G., Hatta, M., Johansen, A. M., Losno, R., Mead, C., Patey, M. D., Swarr, G., Vandermark, A., and Zamora, L. M.: Methods for the sampling and analysis of marine aerosols: Results from the 2008 GEOTRACES aerosol intercalibration experiment, Limnol. Oceanogr. Method., 11, 62–78, https://doi.org/10.4319/lom.2013.11.62, 2013.
Myriokefalitakis, S., Ito, A., Kanakidou, M., Nenes, A., Krol, M. C., Mahowald, N. M., Scanza, R. A., Hamilton, D. S., Johnson, M. S., Meskhidze, N., Kok, J. F., Guieu, C., Baker, A. R., Jickells, T. D., Sarin, M. M., Bikkina, S., Shelley, R., Bowie, A., Perron, M. M. G., and Duce, R. A.: Reviews and syntheses: The GESAMP atmospheric iron deposition model intercomparison study, Biogeosciences, 15, 6659–6684, https://doi.org/10.5194/bg-15-6659-2018, 2018.
Nishikawa, M., Hao, Q., and Morita, M.: Preparation and evaluation of certified reference materials for Asian mineral dust, Glob. Environ. Res., 4, 103–113, 2000.
Nishioka, J. and Obata, H.: Dissolved iron distribution in the western and central subarctic Pacific: HNLC water formation and biogeochemical processes, Limnol. Oceanogr., 62, 2004–2022, https://doi.org/10.1002/lno.10548, 2017.
Nishioka, J., Ono, T., Saito, H., Nakatsuka, T., Takeda, S., Yoshimura, T., Suzuki, K., Kuma, K., Nakabayashi, S., Tsumune, D., Mitsudera, H., Johnson, W. K., and Tsuda, A.: Iron supply to the western subarctic Pacific: Importance of iron export from the Sea of Okhotsk, J. Geophys. Res., 112, C10012, https://doi.org/10.1029/2006JC004055, 2007.
Nishioka, J., Obata, H., and Tsumune, D.: Evidence of an extensive spread of hydrothermal dissolved iron in the Indian Ocean, Earth Planet. Sc. Lett., 361, 26–33, https://doi.org/10.1016/j.epsl.2012.11.040, 2013.
Nishioka, J., Obata, H., Ogawa, H., Ono, K., Yamashita, Y., Lee, K., Takeda, S., and Yasuda, I.: Subpolar marginal seas fuel the North Pacific through the intermediate water at the termination of the global ocean circulation., P. Natl. Acad. Sci. USA, 117, 23, https://doi.org/10.1073/pnas.2000658117, 2020.
Nriagu, J. O. and Pacyna, J. M.: Quantative assessment of worldwide contamination of air, water and soils by trace metals, Nature, 333, 134–139, https://doi.org/10.1038/332141a0, 1988.
Ooki, A., Nishioka, J., Ono, T., and Noriki, S.: Size dependence of iron solubility of Asian mineral dust particles, J. Geophys. Res.-Atmos., 114, 1–8, https://doi.org/10.1029/2008JD010804, 2009.
Pehkonen, S. O., Siefert, R., Erel, Y., Webb, S., and Hoffmann, M. R.: Photoreduction of iron oxyhydroxides in the presence of important atmospheric organic compounds, Environ. Sci. Technol., 27, 2056–2062, https://doi.org/10.1021/es00047a010, 1993.
Pinedo-González, P., Hawco, N. J., Bundy, R. M., and Armbrust, E. V.: Anthropogenic Asian aerosols provide Fe to the North Pacific Ocean, P. Natl. Acad. Sci., 117, 45, https://doi.org/10.1073/pnas.2010315117, 2020.
Radic, A., Lacan, F., and Murray, J. W.: Iron isotopes in the seawater of the equatorial Pacific Ocean: New constraints for the oceanic iron cycle, Earth Planet. Sc. Lett., 306, 1–10, https://doi.org/10.1016/j.epsl.2011.03.015, 2011.
Rathod, S. D., Hamilton, D. S., Mahowald, N. M., Klimont, Z., Corbett, J. J., and Bond, T. C.: A Mineralogy-Based Anthropogenic Combustion-Iron Emission Inventory, J. Geophys. Res.-Atmos., 125, 1–35, https://doi.org/10.1029/2019JD032114, 2020.
Revels, B. N., Zhang, R., Adkins, J. F., and John, S. G.: Fractionation of iron isotopes during leaching of natural particles by acidic and circumneutral leaches and development of an optimal leach for marine particulate iron isotopes, Geochim. Cosmochim. Ac., 166, 92–104, https://doi.org/10.1016/j.gca.2015.05.034, 2015.
Rotman, D. A., Atherton, C. S., Bergmann, D. J., Cameron-Smith, P. J., Chuang, C. C., Connell, P. S., Dignon, J. E., Franz, A., Grant, K. E., Kinnison, D. E., Molenkamp, C. R., Proctor, D. D., and Tannahill, J. R.: IMPACT, the LLNL 3-D global atmospheric chemical transport model for the combined troposphere and stratosphere: Model description and analysis of ozone and other trace gases, J. Geophys. Res.-Atmos., 109, D04303, https://doi.org/10.1029/2002jd003155, 2004.
Sakata, K., Kurisu, M., Tanimoto, H., Sakaguchi, A., Uematsu, M., Miyamoto, C., and Takahashi, Y.: Custom-made PTFE filters for ultra-clean size-fractionated aerosol sampling for trace metals, Mar. Chem., 206, 100–108, https://doi.org/10.1016/j.marchem.2018.09.009, 2018.
Schlitzer, R.: Ocean Data View, available at: https://odv.awi.de (last access: 30 May 2021), 2020.
Schlitzer, R., Anderson, R. F., Dodas, E. M., Lohan, M., Geibert, W., Tagliabue, A., Bowie, A., Jeandel, C., Maldonado, M. T., Landing, W. M., Cockwell, D., Abadie, C., Abouchami, W., Achterberg, E. P., Agather, A., Aguliar-Islas, A., van Aken, H. M., Andersen, M., Archer, C., Auro, M., de Baar, H. J., Baars, O., Baker, A. R., Bakker, K., Basak, C., Baskaran, M., Bates, N. R., Bauch, D., van Beek, P., Behrens, M. K., Black, E., Bluhm, K., Bopp, L., Bouman, H., Bowman, K., Bown, J., Boyd, P., Boye, M., Boyle, E. A., Branellec, P., Bridgestock, L., Brissebrat, G., Browning, T., Bruland, K. W., Brumsack, H. J., Brzezinski, M., Buck, C. S., Buck, K. N., Buesseler, K., Bull, A., Butler, E., Cai, P., Mor, P. C., Cardinal, D., Carlson, C., Carrasco, G., Casacuberta, N., Casciotti, K. L., Castrillejo, M., Chamizo, E., Chance, R., Charette, M. A., Chaves, J. E., Cheng, H., Chever, F., Christl, M., Church, T. M., Closset, I., Colman, A., Conway, T. M., Cossa, D., Croot, P., Cullen, J. T., Cutter, G. A., Daniels, C., Dehairs, F., Deng, F., Dieu, H. T., Duggan, B., Dulaquais, G., Dumousseaud, C., Echegoyen-Sanz, Y., Edwards, R. L., Ellwood, M., Fahrbach, E., Fitzsimmons, J. N., Russell Flegal, A., Fleisher, M. Q., van de Flierdt, T., Frank, M., Friedrich, J., Fripiat, F., Fröllje, H., Galer, S. J. G., Gamo, T., Ganeshram, R. S., Garcia-Orellana, J., Garcia-Solsona, E., Gault-Ringold, M., Grissom, K., Hammerschmidt, C., Hartman, A., Hassler, C. S., Hathorne, E. C., Hatta, M., Hawco, N., Hayes, C. T., Heimbürger, L.-E., Helgoe, J., Heller, M., Henderson, G. M., Henderson, P. B., van Heuven, S., Ho, P., Horner, T. J., Hsieh, Y.-T., Huang, K.-F., Humphreys, M. P., Isshiki, K., Jacquot, J. E., Janssen, D. J., Jenkins, W. J., John, S., Jones, E. M., Jones, J. L., Kadko, D. C., Kayser, R., Kenna, T. C., Khondoker, R., Kim, T., Kipp, L., Klar, J. K., Klunder, M., Kretschmer, S., Kumamoto, Y., Laan, P., Labatut, M., Lacan, F., Lam, P. J., Lambelet, M., Lamborg, C. H., LeMoigne, F. A. C., LeRoy, E., Lechtenfeld, O. J., Lee, J.-M., Lherminier, P., Little, S., López-Lora, M., Lu, Y., Masque, P., Mawji, E., McClain, C. R., Measures, C., Mehic, S., Barraqueta, J.-L. M., vanderMerwe, P., Middag, R., Mieruch, S., Milne, A., Minami, T., Moffett, J. W., Moncoiffe, G., Moore, W. S., Morris, P. J., Morton, P. L., Nakaguchi, Y., Nakayama, N., Niedermiller, J., Nishioka, J., Nishiuchi, A., Noble, A., Obata, H., Ober, S., Ohnemus, D. C., vanOoijen, J., O'Sullivan, J., Owens, S., Pahnke, K., Paul, M., Pavia, F., Pena, L. D., Peters, B., Planchon, F., Planquette, H., Pradoux, C., Puigcorbé, V., Quay, P., Queroue, F., Radic, A., Rauschenberg, S., Rehkämper, M., Rember, R., Remenyi, T., Resing, J. A., Rickli, J., Rigaud, S., Rijkenberg, M. J. A., Rintoul, S., Robinson, L. F., Roca-Martí, M., Rodellas, V., Roeske, T., Rolison, J. M., Rosenberg, M., Roshan, S., RutgersvanderLoeff, M. M., Ryabenko, E., Saito, M. A., Salt, L. A., Sanial, V., Sarthou, G., Schallenberg, C., Schauer, U., Scher, H., Schlosser, C., Schnetger, B., Scott, P., Sedwick, P. N., Semiletov, I., Shelley, R., Sherrell, R. M., Shiller, A. M., Sigman, D. M., Singh, S. K., Slagter, H. A., Slater, E., Smethie, W. M., Snaith, H., Sohrin, Y., Sohst, B., Sonke, J. E., Speich, S., Steinfeldt, R., Stewart, G., Stichel, T., Stirling, C. H., Stutsman, J., Swarr, G. J., Swift, J. H., Thomas, A., Thorne, K., Till, C. P., Till, R., Townsend, A. T., Townsend, E., Tuerena, R., Twining, B. S., Vance, D., Velazquez, S., Venchiarutti, C., Villa-Alfageme, M., Vivancos, S. M., Voelker, A. H. L., Wake, B., Warner, M. J., Watson, R., vanWeerlee, E., AlexandraWeigand, M., Weinstein, Y., Weiss, D., Wisotzki, A., Woodward, E. M. S., Wu, J., Wu, Y., Wuttig, K., Wyatt, N., Xiang, Y., Xie, R. C., Xue, Z., Yoshikawa, H., Zhang, J., Zhang, P., Zhao, Y., Zheng, L., Zheng, X.-Y., Zieringer, M., Zimmer, L. A., Ziveri, P., Zunino, P., and Zurbrick, C.: The GEOTRACES Intermediate Data Product 2017, Chem. Geol., 493, 210–223, https://doi.org/10.1016/j.chemgeo.2018.05.040, 2018.
Schroth, A. W., Crusius, J., Sholkovitz, E. R., and Bostick, B. C.: Iron solubility driven by speciation in dust sources to the ocean, Nat. Geosci., 2, 337–340, https://doi.org/10.1038/ngeo501, 2009.
Shelley, R. U., Morton, P. L., and Landing, W. M.: Elemental ratios and enrichment factors in aerosols from the US-GEOTRACES North Atlantic transects, Deep-Sea Res. Pt. II, 116, 262–272, https://doi.org/10.1016/j.dsr2.2014.12.005, 2015.
Shelley, R. U., Landing, W. M., Ussher, S. J., Planquette, H., and Sarthou, G.: Regional trends in the fractional solubility of Fe and other metals from North Atlantic aerosols (GEOTRACES cruises GA01 and GA03) following a two-stage leach, Biogeosciences, 15, 2271–2288, https://doi.org/10.5194/bg-15-2271-2018, 2018.
Sholkovitz, E. R., Sedwick, P. N., and Church, T. M.: Influence of anthropogenic combustion emissions on the deposition of soluble aerosol iron to the ocean: Empirical estimates for island sites in the North Atlantic, Geochim. Cosmochim. Ac., 73, 3981–4003, https://doi.org/10.1016/j.gca.2009.04.029, 2009.
Sholkovitz, E. R., Sedwick, P. N., Church, T. M., Baker, A. R., and Powell, C. F.: Fractional solubility of aerosol iron: Synthesis of a global-scale data set, Geochim. Cosmochim. Ac., 89, 173–189, https://doi.org/10.1016/j.gca.2012.04.022, 2012.
Stein, A. F., Draxler, R. R., Rolph, G. D., Stunder, B. J. B., Cohen, M. D., and Ngan, F.: Noaa's hysplit atmospheric transport and dispersion modeling system, Bull. Am. Meteorol. Soc., 96, 2059–2077, https://doi.org/10.1175/BAMS-D-14-00110.1, 2015.
Symonds, R. B., Reed, M. H., and Rose, W. I.: Origin, speciation, and fluxes of trace-element gases at Augustine volcano, Alaska: Insights into magma degassing and fumarolic processes, Geochim. Cosmochim. Ac., 56, 633–657, https://doi.org/10.1016/0016-7037(92)90087-Y, 1992.
Tagliabue, A., Bopp, L., Dutay, J.-C., Bowie, A. R., Chever, F., Jean-Baptiste, P., Bucciarelli, E., Lannuzel, D., Remenyi, T., Sarthou, G., Aumont, O., Gehlen, M., and Jeandel, C.: Hydrothermal contribution to the oceanic dissolved iron inventory, Nat. Geosci., 3, 252–256, https://doi.org/10.1038/ngeo818, 2010.
Takahashi, Y., Higashi, M., Furukawa, T., and Mitsunobu, S.: Change of iron species and iron solubility in Asian dust during the long-range transport from western China to Japan, Atmos. Chem. Phys., 11, 11237–11252, https://doi.org/10.5194/acp-11-11237-2011, 2011.
Takahashi, Y., Furukawa, T., Kanai, Y., Uematsu, M., Zheng, G., and Marcus, M. A.: Seasonal changes in Fe species and soluble Fe concentration in the atmosphere in the Northwest Pacific region based on the analysis of aerosols collected in Tsukuba, Japan, Atmos. Chem. Phys., 13, 7695–7710, https://doi.org/10.5194/acp-13-7695-2013, 2013.
Taylor, S. R.: Abundance of chemical elements in the continental crust: a new table, Geochim. Cosmochim. Ac., 28, 1273–1285, https://doi.org/10.1016/0016-7037(64)90129-2, 1964.
Uematsu, M., Duce, R. A., Prospero, J. M., Chen, L., Merrill, J. T., and McDonald, R. L.: Transport of mineral aerosol from Asia over the North Pacific ocean, J. Geophys. Res., 88, 5342–5352, https://doi.org/10.1029/jc088ic09p05343, 1983.
Uematsu, M., Duce, R. A., and Prospero, J. M.: Deposition of atmospheric mineral particles in the North Pacific Ocean, J. Atmos. Chem., 3, 123–138, https://doi.org/10.1007/BF00049372, 1985.
Wang, B. S. and Ho, T. Y.: Aerosol Fe cycling in the surface water of the Northwestern Pacific ocean, Prog. Oceanogr., 183, 102291, https://doi.org/10.1016/j.pocean.2020.102291, 2020.
Wang, Y. F., Huang, K. L., Li, C. T., Mi, H. H., Luo, J. H., and Tsai, P. J.: Emissions of fuel metals content from a diesel vehicle engine, Atmos. Environ., 37(33), 4637–4643, https://doi.org/10.1016/j.atmosenv.2003.07.007, 2003.
Weisel, C. P., Duce, R. A., Fasching, J. L., and Heaton, R. W.: Estimates of the transport of trace metals from the ocean to the atmosphere, J. Geophys. Res., 89, 11607, https://doi.org/10.1029/JD089iD07p11607, 1984.
Wessel, P., Luis, J. F., Uieda, L., Scharroo, R., Wobbe, F., Smith, W. H. F., and Tian, D.: The Generic Mapping Tools Version 6, Geochem. Geophy. Geosy., 20, 5556–5564, https://doi.org/10.1029/2019GC008515, 2019.
Wiederhold, J. G., Kraemer, S. M., Teutsch, N., Borer, P. M., Halliday, A. N., and Kretzschmar, R.: Iron isotope fractionation during proton-promoted, ligand-controlled, and reductive dissolution of goethite, Environ. Sci. Technol., 40, 3787–3793, https://doi.org/10.1021/es052228y, 2006.
Wiederhold, J. G., Teutsch, N., Kraemer, S. M., Halliday, A. N., and Kretzschmar, R.: Iron isotope fractionation in oxic soils by mineral weathering and podzolization, Geochim. Cosmochim. Ac., 71, 5821–5833, https://doi.org/10.1016/j.gca.2007.07.023, 2007.
Wu, J., Rember, R., and Cahill, C.: Dissolution of aerosol iron in the surface waters of the North Pacific and North Atlantic oceans as determined by a semicontinuous flow-through reactor method, Global Biogeochem. Cy., 21, 1–10, https://doi.org/10.1029/2006GB002851, 2007.
Zhang, Y., Wang, X., Chen, H., Yang, X., Chen, J., and Allen, J. O.: Source apportionment of lead-containing aerosol particles in Shanghai using single particle mass spectrometry, Chemosphere, 74, 501–507, https://doi.org/10.1016/j.chemosphere.2008.10.004, 2009.