Magnetic signatures of natural and anthropogenic sources of urban dust aerosol
- 1State Key Laboratory of Loess and Quaternary Geology, Institute of Earth Environment, Chinese Academy of Sciences, Xi'an, 710061, China
- 2College of Earth Science, University of Chinese Academy of Sciences, Beijing, 100049, China
- 3Key Laboratory of Ocean and Marginal Sea Geology, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, Guangzhou, 510640, China
- 4CAS Center for Excellence in Quaternary Science and Global Change, Chinese Academy of Sciences, Xi'an, 710061, China
- 5Research Center for Loess and Global Changes, Institute of Hydrogeology and Environmental Geology, Chinese Academy of Geological Sciences, Shijiazhuang, 050803, China
- 6College of Architecture and Civil Engineering, Beijing University of Technology, Beijing, 100124, China
- 7Institute of Global Environmental Change, Xi'an Jiaotong University, Xi'an, 710049, China
Correspondence: Youbin Sun (firstname.lastname@example.org)
The characteristics of urban dust aerosols and the contributions of their natural and anthropogenic sources are of scientific interest as well as being of substantial sociopolitical and economic concern. Here we present a comprehensive study of dust flux, magnetic parameters, magnetic particulate morphology, and elemental compositions of atmospheric dustfall originating from natural dust sources in East Asia and local anthropogenic sources in Xi'an, China. The results reveal a significant inverse relationship between seasonal variations of dust flux and magnetic susceptibility (χ). By comparing dust flux and χ records, the relative contributions of dust from local anthropogenic sources are estimated. Analyses using scanning electron microscopy (SEM) combined with energy dispersive spectroscopy (EDS) indicate that magnetic particulate from different sources has distinct morphological and elemental characteristics. Detrital magnetic particles originating from natural sources are characterized by relatively smooth surfaces with Fe and O as the major elements and a minor contribution from Ti. The anthropogenic particles have angular, spherical, aggregate, and porous shapes with distinctive contributions from marker elements, including S, Cr, Cu, Zn, Ni, Mn, and Ca. Our results demonstrate that this multidisciplinary approach is effective in distinguishing dust particles derived from distant natural sources and local anthropogenic sources and for the quantitative assessment of contributions from the two end-members.
Urban dust aerosols, comprising both natural and anthropogenic contributions with complex morphological and physiochemical characteristics, have become a focus of study in global climate change and regional air pollution (Wilson et al., 2002). Natural dust is derived primarily from long-range transport with minor local soil contributions and often causes dust events, including sandstorms, suspended dust, and blown-sand weather (Sun et al., 2001; Zhang et al., 2003; Chen et al., 2004; Kan et al., 2007; Baddock et al., 2013); it has an adverse effect on local air quality (Wang et al., 2004; Ginoux et al., 2004). Anthropogenic dust produced by human activities is characterized by high concentrations of toxic heavy metals (e.g., Pb, Zn, Co, Cr, Ni, and As), which has a long-lasting and deleterious impact on the local environment and human health (Zdanowicz et al., 2006; Qiao et al., 2013; Lu et al., 2014; Lee et al., 2015).
Airborne ultrafine particulate matter (e.g., PM2.5 and PM1) can enter the alveolar region and blood circulatory system, leading to health issues and even death (Brunekreef and Holgate, 2002; Nel et al., 2006; Pickrell et al., 2009; Maher et al., 2013; Elser et al., 2016). Moreover, anthropogenic dust is an important medium for the formation of secondary pollutants and plays a significant role in the formation of haze events (Hanisch and Crowley, 2001; Li et al., 2001; Lee et al., 2002; Usher et al., 2002; Finlayson-Pitts et al., 2003; Rubasinghege and Grassian, 2009; Takeuchi et al., 2010; Wu et al., 2011; Huang et al., 2014). Consequently, it is important to distinguish the characteristics and contributions of natural and anthropogenic dust in urban aerosols to formulate effective policies for dust pollution abatement and improving air quality.
Natural and anthropogenic contributions to urban dust aerosols are usually assessed quantitatively using geochemical and magnetic methodologies (Gorden, 1988; Xie et al., 1999; Gomez et al., 2004; Spassov et al., 2004; Kim et al., 2009; Feng et al., 2012). Geochemical methods typically involve source apportionment and the contribution assessment of representative heavy metal elements using statistical methods such as chemical mass balance (CMB) (Chow et al., 2002; Gupta et al., 2007) and factor analysis (FA) (Harrison et al., 1997a; Salvador et al., 2004). Pb, Fe, Zn, Cr, Cd, Ni, Ba, and Sb are frequently used as marker elements for vehicle emissions (Huang et al., 1994; Adachi and Tainosho, 2004; Meza-Figueroa et al., 2007), while Hg, Pb, Mn, Cr, Co, Cu, Cd, and Ni are regarded as indicators of coal combustion (Vouk and Piver, 1983; Pacyna and Pacyna, 2001; Sushil and Batra, 2006).
Since magnetic measurements are rapid, inexpensive, and nondestructive, environmental magnetism is increasingly being used as an effective approach to study urban dust pollution (Maher, 1998; Hoffmann et al., 1999). By combining magnetic properties with morphological features (Muxworthy et al., 2001; Urbat et al., 2004; Blaha et al., 2008a) as well as heavy metal (Hunt et al., 1984; de Miguel et al., 1997; Blaha et al., 2008b; Maher et al., 2008) and back-trajectory characteristics (Wehner et al., 2008; Li et al., 2009; Fleming et al., 2012), the provenance, transport routes, and spatial distribution of polluted dust aerosols can be investigated. This multidisciplinary approach is becoming a popular means of urban pollution monitoring and assessment (Jordanova et al., 2014; Stein et al., 2015; Yan et al., 2015a; Bourliva et al., 2016).
Using environmental magnetic techniques to assess pollution levels and sources, different forms of urban dust aerosols in East Asia have been studied, including atmospheric dustfall, street dust, leaf dust, inhalable particulate matter, and surface soil. For example, spatial and temporal pollution patterns were quantitatively estimated from seasonal fluctuations of the concentration and grain size of magnetic particles in urban roadside dust (Kim et al., 2007, 2009). A high correlation between magnetic parameters (magnetic susceptibility and saturation isothermal remanence, i.e., χ and SIRM) and heavy metal concentrations in street dust, polluted farmland soil, and atmospheric dustfall was observed, indicating that these magnetic parameters can be employed as effective proxies to assess heavy metal pollution (Zhang et al., 2011, 2012a, b; Qiao et al., 2013). SIRM characteristics of roadside leaves were shown to reflect spatial variations of magnetic particles in urban dustfall (Quayle et al., 2010; Hansard et al., 2011, 2012; Maher et al., 2013; Kardel et al., 2012). Although morphology, grain size, mineral, and element analyses were utilized in previous works, there are no studies that systematically compare magnetic signatures of natural dust, urban dust aerosol, and polluted dust from source to sink.
This study systematically collected surface sediments from potential dust sources in East Asia, urban dust aerosols in Xi'an, including atmospheric dustfall (over five consecutive years) and street dust, and typical anthropogenic pollutants such as vehicle exhaust and fly ash. Morphology and elemental compositions of magnetic particles in representative samples were analyzed to facilitate a thorough source–sink comparison. Our results indicate that natural and anthropogenic contributions to urban dust aerosols can be differentiated using a combination of their magnetic, morphological, and elemental characteristics.
Surface sediments were collected in potential dust source regions of East Asia, including the northern Chinese deserts (the Badain Juran and Tengger Desert), the Taklimakan Desert, Mongolian Gobi, and Tibetan Plateau (Fig. 1a). Fine-grained materials were collected from alluvial fans, dry riverbeds, lake basins, and drainage depressions within Gobi–sandy deserts at intervals of 100 to 200 km (Fig. 2a–d). To better understand the different sedimentary characteristics, 48 samples from the northern Chinese deserts, 50 samples from the Taklimakan Desert, 23 samples from the Mongolian Gobi, and 32 samples from the Tibetan Plateau were selected for magnetic measurements. Locations of the samples are shown in Fig. 1a. Detailed descriptions were given in Sun et al. (2013).
A total of 68 street dust samples were collected from parks, construction sites, commercial streets, and residential areas in Xi'an following a 3×4 km grid spanning approximately 30 km from west to east and 20 km from north to south (Fig. 1b). The sampling grid covers a range of different functional areas in Xi'an, including the Industrial District, Commercial District, Cultural District, Ecological District, and Han Chang'an city ruins park. We also collected four typical anthropogenic pollutant samples in June 2017, including one sample of exhaust from several vehicles, one sample of fly ash from a dust bag of electrostatic precipitators at the Baqiao thermal power plant, one street dust sample from the Bell Tower in downtown Xi'an, which experiences daily traffic jams, and one street dust sample near the Baqiao thermal power plant where coal burning is the leading pollution factor. The locations of these samples are shown in Fig. 1b.
Atmospheric dustfall collectors were placed on the top of a four-story building at the Institute of Earth Environment, Chinese Academy of Sciences, ∼10 m above the ground surface, and a 15-story building inside the Xinxinjiayuan residential community, ∼50 m above the ground surface (Fig. 2e, f). The sampling sites situated in southwest Xi'an consist primarily of commercial and residential districts. Samples were collected using the wet-collection method (Qian and Dong, 2004) at time intervals of 3–5 days in spring and 6–7 days in other seasons. Detailed sampling procedures were reported by Yan et al. (2015a, b); 733 samples were collected from March 2009 to March 2014. Dust flux (DF, g m−2 day−1) is calculated as follows:
where W is the sample weight in g, A is the area in m2, and T is sampling duration in days.
Low- and high-frequency magnetic susceptibilities (χlf and χhf, respectively) are measured using a MFK1-FA Kappabridge at frequencies of 976 and 15 616 Hz. Frequency-dependent magnetic susceptibility (χfd) is calculated as (χlf−χhf) / χlf×100 %.
The temperature-dependent susceptibilities (χ−T) are measured in an argon atmosphere (the flow rate is 50 mL min−1) at a frequency of 976 Hz from room temperature up to 700∘ and back to room temperature using a MFK1-FA Kappabridge equipped with a CS-3 high-temperature furnace. The susceptibility of each sample is corrected for background (furnace tube correction) using the CUREVAL 8.0 program.
Hysteresis loops and first-order reversal curve (FORC) diagrams are measured by a vibrating sample magnetometer (VSM3900) to a maximum applied field of 1 T. Hysteresis parameters, including the saturation magnetization (Ms), saturation remanent magnetization (Mrs), and coercivity (Bc), are obtained after subtracting the paramagnetic contribution. The remanence coercivity (Bcr) is obtained by demagnetizing samples from +1 T back to −1 T. The hysteresis ratios Mrs∕Ms vs. Bcr∕Bc are used to construct a Day plot.
The FORC diagrams are measured with the averaging time of 200 ms and produced using FORCinel software (Harrison and Feinberg, 2008). A total of 18 samples are used for detailed iron oxide analyses, including 2 samples from each natural dust source with modal χlf values, 4 dustfall samples and 2 street dust samples with high χlf and low χlf, and 2 samples of vehicle exhaust and fly ash.
The magnetic components of these representative samples are separated from the bulk samples using a 1 T magnet sealed in a polyethylene bag. To confirm their mineral, morphological, and elemental characteristics, direct observations and measurements of the samples and their extracted magnetic particles are performed using a ZEISS EVO-18 scanning electron microscope (SEM) equipped with a Bruker XFlash 6130 energy dispersive spectroscope (EDS). Samples are mounted on the SEM stub with double-sided carbon tape and then coated with a thin gold film. The specified resolution of the SEM is <5 nm. The EDS detector is capable of detecting elements with atomic numbers ≥5 and the detection sensitivity can reach 0.1 wt%. Bulk samples and magnetic extracts are characterized by randomly selecting three to four fields of view and examining all the particles observed within the selected fields. All the measurements are made at the Institute of Earth Environment, Chinese Academy of Sciences, Xi'an.
3.1 Magnetic mineralogy
χ−T is used to identify magnetic mineral composition. All the χ−T heating curves (Fig. 3a–f) are characterized by a major susceptibility decrease at 580∘, i.e., the Curie temperature of magnetite, which identifies magnetite as the major contributor to χ. All the samples are irreversible with cooling paths above heating trajectories due to the neoformation of magnetite (Jordanova et al., 2004; Kim et al., 2009). The χ−T heating curve of the vehicle exhaust displays a decreasing χ between 580 and 700∘ (Fig. 3b), suggesting the presence of hematite.
All samples have similar slightly wasp-waisted hysteresis loops (Fig. 3g–l). Magnetic saturation is generally reached at a magnetic field of about 300 mT. This is a clear indication of the predominance of low-coercivity ferrimagnetic minerals in all samples.
3.2 Hysteresis properties
The Day plot and FORC diagram are powerful methods to identify the domain state distribution of magnetic materials (Day et al., 1977; Pike et al., 1999; Roberts et al., 2000; Dunlop, 2002a, b). All the samples agree well with single-domain + multi-domain admixture curves in the pseudo-single-domain range of the Day plot (Fig. 4a). The FORC diagrams for street dust (Fig. 4d) and anthropogenic pollutants (Fig. 4e) have divergent contours that are characteristic of multi-domain grains. The FORC diagram for natural surface sediments (Fig. 4b) seems to be characteristic of pseudo-single-domain and multi-domain behavior, whose outer contours display a divergent pattern and inner contours are somewhat less divergent. The FORC distributions of atmospheric dustfall (Fig. 4c) appear to have a mixed set of contours. The outer contours have a divergent pattern that would be expected for multi-domain particles, while the inner distribution with closed contours represent single-domain grains.
3.3 Spatial and temporal variations of χ
The magnetic susceptibilities of all bulk samples were measured to estimate concentrations of magnetic minerals, which are largely controlled by concentrations of ferromagnetic minerals (Dunlop and Özdemir, 1997; Evans and Heller, 2003; Liu et al., 2012). χfd is sensitive to the superparamagnetic component. There are virtually no superparamagnetic grains when χfd is <2 %, while a mixture of superparamagnetic and coarser grains is indicated with χfd in the range of 2–10 % (Dearing, 1994; Dearing et al., 1996). The peaking of the χlf frequency distribution curve indicates the χlf values are most distributed in this interval. Both χlf and χfd exhibit a distinctive distribution pattern in different sources.
χlf values from the Taklimakan Desert and northern Chinese desert samples exhibit a unimodal distribution (Fig. 5a), and those from the Mongolian Gobi exhibit a bimodal distribution. However, χlf values have a multimodal distribution in the Tibetan Plateau (Fig. 5a). Different distribution patterns and peak values of χlf (Fig. 5a) indicate that the assemblage of magnetic minerals may differ in these four natural sources. Average χlf in individual sources shows a decreasing trend from the Mongolian Gobi, to northern Chinese deserts and the Tibetan Plateau, and then to the Taklimakan Desert (Fig. 5e). The mean values of χfd in different natural sources show a decreasing trend of superparamagnetic components from the Taklimakan Desert to Mongolian Gobi and Tibetan Plateau, and then to northern Chinese deserts (Fig. 5f).
The frequency distributions of χlf for the street dust and atmospheric dustfall are both unimodal (Fig. 5c). The average χlf and χfd values of the street dust are higher than those of the atmospheric dustfall and natural surface sediments (Fig. 5e). Low χlf ( m3 kg−1) occurs in the Ecological District, Han Chang'an city ruins park, and Cultural District, while samples with intermediate χlf values (500– m3 kg−1) are from the moderately developed Industrial District and the periphery of the Commercial District. In contrast, the central areas of the Industrial District and the Commercial District (particularly the area of high traffic density at the Bell Tower) are characterized by relatively high χlf values ( m3 kg−1). χlf of atmospheric dustfall from XA1 and XA2 exhibits significant and consistent seasonal variations (Fig. 6). The lowest (highest) χlf values correspond to the highest (lowest) dust flux in spring (autumn).
The representative anthropogenic pollutants, i.e., vehicle exhaust, fly ash, and nearby street dust at the Bell Tower and thermal power plant, have high χlf and χfd (Fig. 5c, d). The χlf and χfd of vehicle exhaust and fly ash are higher than the mean values of other sources of dust (Fig. 5e, f).
3.4 Morphology and mineralogy of the dust samples
SEM provides morphology information based on gray-scale intensity. The elemental composition is determined by the EDS detector. In order to compare the morphology and mineralogy characteristics of different dust aerosols, more than 40 fields of views of the representative bulk samples were randomly obtained for various types of particles. The morphologies and mineral compositions of the natural surface sediments, street dust, and atmospheric dustfall with low and high χlf are illustrated in Fig. 7. The particles are typically angular and irregularly shaped in the surface sediments, with a broad size range (around 1–100 µm). Based on the EDS analysis for each particle in the selected field, clay minerals, quartz, calcite, dolomite, and magnetic grains (Fig. 7a) were clearly identified (Welton, 1984).
The SEM–DES analysis shows that the morphology and constituents of the particles in the street dust are complex and heterogeneous. Three categories of particles can be morphologically differentiated, including irregular and aggregate mineral particles, spherical particles, and anomalous particles with porous and loose structures (Fig. 7b). Particles with irregular shapes are mainly minerals and commonly present in street dust samples. Compared to the natural surface sediments, the grain size of mineral particles in the street dust is finer and mostly ranges from 1–50 µm, with some up to 80 µm. Spherical particles are mainly amorphous silicon–aluminum and iron-rich spheres, whose grain size varies mostly from 1–20 µm, with some up to 50 µm. There are a small number of anomalous particles with diameters of 10–100 µm.
The morphology and mineral composition of atmospheric dustfall are similar to those of the street dust, except that atmospheric dustfall with low χlf has a higher content of irregularly shaped detrital minerals (Fig. 7c), while that with high χlf contains more spherical and anomalous particles (Fig. 7d).
3.5 Elemental compositions of mineral particles
Since the elemental compositions of mineral particles can be clearly distinguished using SEM–EDS analysis (Blanco et al., 2003; Kutchko and Kim, 2006), a street dust sample dominated by anthropogenic inputs with the highest χlf was selected for EDS analysis. The results indicate that various mineral particles exhibit distinct chemical compositions (Fig. 8). The plate-like aggregates (labeled a) with high levels of Si and Al and low levels of K, Ca, Mg, and Fe are clay minerals composed of crystalline sheet-structure silicates with a small particle size (Fig. 8a). The angular and sharp-edged particle (labeled b) with high Si and O is quartz (Fig. 8b). The angular particle consisting of Si, Al, and K is potassium feldspar (Fig. 8c). Particles with high levels of Ca and Mg are calcite (Fig. 8d) and dolomite (Fig. 8e).
The irregular particles (labeled f) that are abundant in Fe are identified as magnetic grains (Fig. 8f), although some of the particles show low levels of crustal elements, including Si, Al, Ca, and K. Two types of spheres were observed. One (labeled g) is an amorphous aluminosilicate particle (Fig. 8g) with predominant Si and Al and lesser amounts of K, Mg, Na, and Ti. The other (labeled h) is an iron-rich sphere (Fig. 8h), which is mainly composed of Fe. These particles exhibit various surface textures. In addition, almost all particles contain O and C.
4.1 Contributions of local anthropogenic sources estimated by dust flux and χlf
On the bivariate plot of χlf vs. χfd, atmospheric dustfall is intermediate between the surface sediments and street dust (Fig. 9b), implying that atmospheric dustfall is a mixture of distal natural dust and local anthropogenic dust, but much closer to the latter. The local anthropogenic contribution (LC) is mainly derived from local stable and sustained pollutant sources, including vehicle emissions and fly ash. Considering that natural dust comes primarily from natural dust sources with a minor local soil contribution (Wang et al., 2004; Ginoux et al., 2012), we attribute the natural contribution entirely to the distal natural dust.
The dust flux background can be taken as the average input from the end-member of LC. The time-dependent background estimation was calculated using
where , x(i)bg is the background of x(i) at time t(i). MED is the running median with window points of 2k+1 ( (Härdle and Steiger, 1995); cross-validation can be used to choose k. We used two such criteria: the median criterion (Zheng and Yan, 1988) and L1 norm (Marron, 1986; Dodge, 2012).
MED is the delete-one background estimate. The cross-validation functions are to measure the average performance of the delete-one estimate to predict the observation x(i). Optimal k values should minimize CVm(k) or CV1(k) (Mudelsee, 2006).
Through the cross-validation calculation on the dust flux series of atmospheric dustfall, we find that the cross-validated number of window width (Eq. 3) is k=19. On this basis, we calculate the monthly LC using the ratio of monthly background and total dust flux as
where LCflux is the percentage of the monthly local anthropogenic contribution estimated by dust flux (Fig. 10a). Note that when the background is larger than the dust flux, LC is taken to be 100 %.
Ms values of representative samples (Fig. 3h–m) are measured to identify the concentration of ferrimagnetic minerals. We find that the averaged values of Ms in different sources show a rising trend from the natural surface sediments (0.04 Am2 kg−1) to atmospheric dustfall (0.81 Am2 kg−1) and street dust (1.03 Am2 kg−1), and then to anthropogenic pollutants (1.58 Am2 kg−1), which correspond to the characteristics of averaged χlf in different sources. This indicates that the high χlf of urban dust is caused by ferrimagnetic minerals from a local anthropogenic source. In consequence, the LC contribution could also be estimated by the peak values of χlf frequency distribution, with 20– m3 kg−1 in the distant natural surface sediments and 500– m3 kg−1 in local street dust (Fig. 9a). On this basis, we calculate the average LC using the following equation:
where LCχ is the percentage of the monthly local contribution estimated by χlf (Fig. 10b), and χm is the monthly average χlf value in 10−8 m3 kg−1. and m3 kg−1 are the average χlf values of surface sediments from source regions and local street dust, respectively. Note that when χm is larger than the average χlf of the street dust, LC is taken to be 100 %.
The LCflux and LCχ values have the same trend and show a distinctive seasonal pattern (Fig. 10a, b), with a maximum in autumn (92.4 %, 92.3 %), followed by winter (90.8 %, 74.7 %), summer (83.5 %, 71 %), and spring (73.0 %, 53.1 %). Both the LCflux and LCχ are the lowest in spring, implying that distant natural dust input makes a great contribution to atmospheric dustfall during this period.
The LC variation exhibits a similar seasonal pattern to χlf, but an opposite trend to that of dust flux (Fig. 10a, b). This suggests that the major sources of atmospheric dustfall varied seasonally between the distant natural sources in spring and local anthropogenic sources in other seasons. In spring, dust is emitted from the natural sources by strong winds, and after long-range transport it contributes to the elevated dust flux in Xi'an and decreases the LC in atmospheric dustfall. However, from summer to winter, dust input from local anthropogenic sources is low and stable as indicated by the high LC.
4.2 Magnetic characteristics of anthropogenic particles
SEM–EDS analysis shows that the extracted magnetic particles from the street dust and atmospheric dustfall can be divided into detrital and anthropogenic types (Fig. 11a–c). Detrital particles are angular and characterized by relatively smooth surfaces, with Fe and O as the major elements and minor amounts of Ti (Fig. 11d), indicating the presence of magnetite, hematite, and titanomagnetite (Maher and Thompson, 1991; Liu et al., 2015). Anthropogenic particles include angular particles with coarse surface textures, spherules, aggregates, and porous particles with complex internal structures. The major elements identified in these particles are Fe and O, which indicate the occurrence of magnetite or hematite, consistent with previously identified anthropogenic magnetic particles (Kim et al., 2007; Koukouzas et al., 2007; Maher, 2009). Minor concentrations of S, Zn, Cu, and Cr were also observed in this type of particle, which is typically attributed to anthropogenic activities (Fig. 11d). The relatively weaker signal intensity of Fe in the EDS spectra of porous particles indicates a much lower Fe concentration (maximum less than 10 %), while their concentrations of Si, Al, Ca, Ti, and Mn are higher.
The morphology and concentration of magnetic materials in urban dust aerosols varied with sampling sites and over time. Among more than 20 images of analyzed magnetic extracts from urban dust samples, angular particles with coarse surface textures were the most frequently observed (>50 %, some up to 80 %), with a wide range of grain size (1–100 µm). Spherules were also commonly observed in all samples, ranging from 10–40 %, mainly with diameters from 10–30 µm. Aggregates with diameters of 5–30 µm account for less than 10 %. Detrital particles characterized by smooth surfaces range from 1–5 % and have small diameters (1–20 µm). Porous particles are the least observed magnetic particles (<1 %) with diameters of 30–120 µm. The SEM–EDS data show that the morphology and concentration of magnetic particulates in atmospheric dustfall with high χlf values are similar to those of the street dust, whereas atmospheric dustfall with low χlf contains more angular–subangular magnetic particles of detrital origin.
4.3 Potential sources of anthropogenic magnetic particles
Anthropogenic magnetic particles in the urban environment are mainly derived from the combustion of fossil fuels (Flanders, 1994; Matzka and Maher, 1999; Muxworthy et al., 2001), vehicle emissions (Harrison et al., 1997b; Moreno et al., 2003; Diapouli et al., 2008; Pant and Harrison, 2013; Maher et al., 2013), and industrial activities (Hanesch et al., 2003; Desenfant et al., 2004). To clarify potential sources, microscopic and elemental investigations of magnetic extracts from anthropogenic pollutants were performed using SEM–EDS. Compared with the magnetic particles in atmospheric dustfall (Fig. 12a–d), those from vehicle exhaust consist of only three types of particles, including angular particles with coarse surface textures, spherules, and aggregates (Fig. 12e–g), while all magnetic particle types in dustfall samples were identified in fly ash (Fig. 12h–k). The EDS analysis showed that the major elements of the same three types of magnetic particles in vehicle exhaust and fly ash are Fe and O, consistent with elemental features of those in atmospheric dustfall (Fig. 12l–n). This suggests that vehicle exhaust and fly ash are the main pollutant sources in dustfall. However, there are some differences in the compositions of the minor elements in the three types of particles between vehicle exhaust and fly ash. Angular particles with coarse surface textures from vehicle exhaust contain more S, Cr, Cu, Zn, and Mn, while those from fly ash have more Ca and Mn. Aggregates consist of more Cr, Zn, and S in vehicle exhaust, whereas Ca and S are enriched in fly ash. Spherules from vehicle exhaust contain higher amounts of heavy metals (Cr, Ni, Mn, and Zn), while those from fly ash have higher Ca and Mn. Coarse-grained porous magnetic particles were only observed in fly ash, which are relatively low in Fe and high in crustal elements (e.g., Si, Al, K, Ca, Mg, and Ti).
The EDS elemental data clearly indicate that the magnetic particles from vehicle exhaust contain higher concentrations of a greater range of elements from anthropogenic activities (S, Cr, Cu, Zn, Ni, and Mn) than those from fly ash, whose EDS spectra show a substantial peak of Ca. The χlf ( m3 kg−1) and Ms (2.5 Am2 Kg−1) values of vehicle exhaust are significantly higher than those of fly ash ( m3 kg−1 and 0.66 Am2 Kg−1), indicating a higher content of ferrimagnetic contaminants. In summary, the magnetic particles emitted by vehicle exhaust and thermal power plants can be distinguished by a combination of morphological and elemental characteristics, which indicates that SEM–EDS can be used to trace the sources of anthropogenic pollutants in Xi'an.
By comparing the magnetic properties of surface sediments in natural dust sources in East Asia and various urban dust samples in Xi'an, we found that distal natural dust and local anthropogenic dust have different magnetic, morphological, and elemental characteristics. We take natural surface sediments as representative of distal natural dust, with background atmospheric dustfall and polluted street dust as representative of local anthropogenic dust. Based on this end-member configuration, the relative contributions of local anthropogenic sources to urban atmospheric dustfall can be quantitatively estimated.
The results show that local anthropogenic contribution decreases in spring and increases in other seasons. Local anthropogenic contribution variation exhibits a similar seasonal pattern to χlf, but an opposite trend to that of dust flux with a maximum in spring. This means that a great amount of distant natural dust input with less magnetic content makes a great contribution to atmospheric dustfall in spring, which results in minimum χlf and anthropogenic contributions during this period. Hence, the local contribution is reduced as a result of increasing natural dust flux.
SEM–EDS analysis of urban dust indicates that magnetic particles produced by anthropogenic activities have distinct morphological and elemental characteristics. The anthropogenic particles exhibit angular, spherical, aggregate, and porous shapes and contain distinctive marker elements such as S, Cr, Cu, Zn, Ni, Mn, and Ca. The porous particles are likely derived from the thermal power plant, while others may be attributed to both vehicle exhaust and the thermal power plant. Our results suggest that magnetic signatures combined with morphological and elemental compositions can be used to quantitatively estimate local and anthropogenic contributions to urban dust aerosols.
All relevant data are accessible for the public on the website http://paleo-data.ieecas.cn (last access: 10 January 2019; China IEECAS, 2009). One can also contact the author for access.
HL and YS designed the study and collected urban dust aerosols. YY, LL, HC, and XL performed the fieldwork. HL and YY contributed to dust flux analysis. HL and HC conducted the morphology and mineralogy experiments. XQ analyzed the magnetic data. All authors contributed to discussion, interpretation of the results, and writing the paper.
The authors declare that they have no conflict of interest.
We thank Min Zhao and Hua Wang for the help in sample
collection. We are also grateful for the help of Maojie Yang with SEM–EDS
measurements and Jan Bloemendal with language polishing. This work was
supported by the National Key Research and Development Program of China
(2016YFA0601902) and the Open Foundation of State Key Laboratory of Loess
and Quaternary Geology (SKLLQG1631).
Edited by: Patrick Chuang
Reviewed by: two anonymous referees
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