Distribution of soil selenium in China is potentially controlled by deposition and volatilization?



Elucidating the environmental drivers of selenium (Se) spatial distribution in soils at a continental scale is essential to better understand it’s biogeochemical cycling to improve Se transfer into diets. Through modelling Se biogeochemistry in China we found that deposition and volatilization are key factors controlling distribution in surface soil, rather than bedrock-derived Se (<0.1 mg/kg). Wet deposition associated with the East Asian summer monsoon, and dry deposition associated with the East Asian winter monsoon, are responsible for dominant Se inputs into northwest and southeast China, respectively. In Central China the rate of soil Se volatilization is similar to that of Se deposition, suggesting that Se volatilization offsets it’s deposition, resulting in negligible net Se input in soil. Selenium in surface soil at Central China is roughly equal to low petrogenic Se, which is the main reason for the presence of the Se poor belt. We suggest that both deposition and volatilization of Se could play a key role in Se balance in other terrestrial environments worldwide.


Selenium (Se) is an essential micronutrient for humans1,2, and most Se is primarily derived from cereals, including through secondary consumption as meat1,2,3. In general, the accumulation of Se in edible part of plants is highly dependent on Se level in soils2,4. In China, human Se deficiency is associated with chronic bone and cartilage disease (Kashin-Beck disease) and chronic heart disease (Keshan Disease)5,6. These diseases are found in populations living in the Se-poor belt in Central China, which stretches from northeast (Heilongjiang Province) to southwest (Yunnan Province) (Fig. 1A).

Figure 1

Distribution pattern of soil selenium concentration and desert (A), and wet deposition (B) in China (China Meteorological Data Sharing Service System, China’s precipitation data of 1971–2000. http://cdc.nmic.cn/home.do). The maps were created using Arc GIS Geographic Information Systems software version 10.2 (Environmental Systems Research Institute Inc, Redlands, Calif).

Chinese agricultural regions are divided into two broad catchments according to the 400 mm isohyets, an important geographical boundary for summer monsoon limit (Fig. 1B). The west belonging to semi-arid (200–400 mm) or arid climate (<200 mm), is dominated by grassland and the east belonging to semi-humid (400–800 mm) or humid (>800 mm), dominated by arable farming. The extensive Se-poor belt is located in the eastern farming region and accounts for ~70% of Chinese arable land7. Extremely low Se in soils within this general Se-poor belt results in widespread Se deficiency in edible produce, which poses a human health risk for ~0.7 billion inhabitants of this area7.

At large geographical scales the spatial distribution of Se in the terrestrial environment is poorly understood8. Previous studies mainly focused on the transformation and biogeochemical cycling of Se in soils at micro-scale7,9. It is generally accepted that on the regional scale soil-forming parent materials or rocks are among the most important factors affecting Se distribution in soils6,8. However, on the national scale such as in China, it remains elusive as to what are the predominant factors in regulating Se distribution (Fig. 1).

Generally, crystalline bedrock and Quaternary sediments have been identified as the major parent materials for soil10. The surface bedrock of earth is covered by 75% sedimentary rock and 25% metamorphic and igneous rocks. In China about 77.3% of total area is covered by sedimentary rocks (Fig. 2). Except for some organic-rich rock such as black shale and volcanic emanations, most types of rock contain relatively low Se, roughly in the similar range of Se with crustal abundance11. The average crustal abundance of Se worldwide is estimated to be 0.05–0.09 mg/kg8. In China, the average abundance of Se in the earth’s crust is 0.058 mg/kg, a bit lower than that in other parts of the world12. The Se concentration of various rock types in China is 0.07 mg/kg in metamorphic rocks, 0.067 mg/kg in igneous rocks, and 0.047 mg/kg in sedimentary rocks12. The maps of soil parent materials and distribution of soil Se in China should be matched each other if rock-derived Se from parent materials are the main contributor of soil Se, but they do not (Figs 1A and 2). This must mean that the spatial variability of soil Se distribution is affected by other factors besides low Se in soil-forming parent materials or rocks. The mean Se concentrations in soils in northwestern China (Se-adequate region), the middle part (Se-poor belt), and the southeastern part (Se-adequate region) are 0.19, 0.13 and 0.23 mg/kg, respectively5. A comparison between the average Se content in different parts of Chinese soils and the average Se concentration in Chinese earth’s crust (0.058 mg/kg) indicates other factors play an important role in elevating Se concentrations in surface soil.

Figure 2: Map of soil parent material and rock of China from a book titled “The atlas of soil environmental background value in the People’s Republic of China”. 1994, page 10–11, China Environmental Science Press.

The maps were modified using Arc GIS Geographic Information Systems software version 10.2 (Environmental Systems Research Institute Inc, Redlands, Calif).

One source of Se in soil besides parent rocks could be the atmospheric deposition13,14,15,16,17. Dissolved Se in seawater was taken up by phytoplankton and transformed to gaseous Se compounds in marine environments. Significant concentrations of gaseous Se occur in surface ocean waters and emit to the atmosphere17,18. Marine derived Se is thought to be an important source of Se to terrestrial ecosystems14,15,16,18. Countries closer to the ocean tend to have more sufficient Se supply in soil than those in central Europe9. High wet deposition was accompanied by high soil Se in southeast China (Fig. 1B), suggesting wet deposition derived from East Asian monsoon is one of the important controlling factors of Se distribution in China19. The deposition in Central China is relatively low and geographically coincides with the Se-poor belt (<0.1 mg/kg). Surface soil Se concentration in this region is similar to or slightly higher than Se level in bedrock, much less than that in Northwest or Southeast China, indicating that Se accumulation in surface soil was limited. Monsoonal deposition is an important Se input19 and no major Se output was documented, the Se levels in surface soil of Se-poor belt would be progressively increased rather than similar to petrogenic Se level (<0.1 mg/kg). Mechanisms for formation of the Se poor belt in this region remained elusive. In Northwest China, which beyond the range of the East Asian summer monsoon, wet deposition is much less (<200 mm), even less than 100 mm in some regions such as the Gobi desert20. However, the high Se in surface soils was observed (Fig. 1A). Obviously, the elevation of Se in northwest China is not due to transport and deposition from the East Asian summer monsoon.


Selenium input from wet deposition

Annual mean wet deposition decreases gradually from 2,000 mm along the southeastern coast, to 400–800 mm in central China, and less than 200 mm in most of the Northwest (Fig. 1B). According to the deposition gradient derived from Southeast Asia summer monsoon in China, the whole territory can be divided into 3 regions: 1) Southeast humid region (>800 mm); 2) Central dry and humid region (400–800 mm); and 3) Northwestern dry region (<400 mm, beyond summer monsoon) (Fig. 1B). In Southeast humid region, the highest frequency of Se concentration in inland deposition of China is in the range of 0.1–0.2 μg Se/L8,21, similar to the average value of the deposition samples (0.21 μg Se/L) in UK22. Based on the concentrations of Se in rainwater, the Se depositions in the soil at different rainfall were calculated (Table 1).

Table 1 Calculated Se deposition, volatilization and net input (deposition minus volatilization) in soil.

Following the increase of rainfall (deposition>800 mm) the Se concentration was substantially enhanced in the southeast humid soil region in comparison with Se contents in the bedrock (0.047–0.07 mg/kg). Wet deposition associated with East Asian summer monsoon has been suggested as a major contributor to the distribution of trace elements23. The largest natural source of Se to the atmosphere was marine biogenic origin15,16, up to 60–80% of the atmospheric Se14. Gaseous Se derived from oceanic emission is transported through the atmosphere and deposited to terrestrial environments18,24,25. When wet deposition is 2,000 mm annually, the Se input in the surface soil was up to 200–400 μg/m2 per year (Table 1).

Central dry and humid regions (400–800 mm) geographically coincide with the Se-poor belt (Fig. 1). The amount of Se deposited by deposition is highly dependent on distance from the ocean. This region is far from ocean Se source and deposition of Se is much less. According to the calculated Se deposition (Table 1), the rate of Se deposition in this region is 40–160 μg/m2/yr.

Selenium input from dry deposition

The Northwestern dry region (<400 mm) exhibit high Se, especially in the arid environment with annual deposition less than 200 mm although no deposition of East Asian summer monsoon occurred. The distribution of Se in this region is surprisingly coincident with the distribution of desertified lands (Fig. 1A). The East Asian monsoon, the largest monsoon system, is an important part of global atmospheric circulation. Unlike African and Indian monsoon, the East Asian monsoon is divided into a warm and wet summer monsoon and a cold and dry winter monsoon, which is a unique and strong winter circulation. Main features of the winter monsoon in East Asia are that very strong high-pressure and low-pressure systems form over the Mongolia and Siberia (High) and the northern Pacific Ocean (Low), respectively. This cold and dry winter monsoon is not only the most powerful winter monsoon worldwide, but also responsible for the mineral dust deposition (Fig. 1B). Asian winter monsoon generates wind patterns in winter that sweep clastic material from the deserts of the Central Asian and deposits it in China. Three areas including deserts in Mongolia, Taklimakan and Badain deserts in western and northern China have been concluded to be the major sources for Asian mineral dust, contributing ~70% of the total dust emitted26. The mean rates of dust deposition were 200 g/m/yr at local scale (0–10 km from dust source) and 20 g/m/yr at regional scale (10–1000 km from dust source) respectively, much higher than that (0.4 g/m/yr) at global scale (>1,000 km from dust source)26,27. Most desertified lands in Northwestern China are located at local scale or regional scale from dust source. Much of the mineral dust raised (~30%) in Asia was redeposited onto the deserts including Gobi, desertified land and potential desertified land (Fig. 1A)28.

The total dust production from Chinese deserts is estimated ~ 800 Tg/yr into the atmosphere with a range of 500–1,100 Tg/yr28, accounting for half of the global dust production of 1500 Tg/yr29 or 1,000–2,000 Tg/yr30. Global Se dry deposition has been estimated to be 1.7–2.4 × 109 g Se per year, less than wet deposition of 3.5–10.0 × 109 g Se per year31. Northwestern dry region is close to the deserts (the source of deposition in Asia). Aerosol concentration of Se has been demonstrated to be highly enriched relative to average crustal abundances32. It is plausible explanation that on most desert margins high Se (>0.4 mg/kg) was accumulated in surface soil due to dry deposition (Fig. 1A). Obviously, dry deposition associated Asian winter monsoon is major contributor for Se elevation in in northwest China.

Selenium volatilization to decrease soil Se

Selenium volatilization from soil is one of the most important processes of Se biogeochemical cycling in terrestrial environments33. Dimethylselenide and dimethyl diselenide are the major volatile Se species emitted to the air from soil31. Biological volatilization is regarded as a significant pathway of Se removal in wetlands31.

It has been shown that volatilization of Se from soils can be influenced by various factors, including temperature34,35,36, soil moisture35,36,37, and organic C sources37,38. Many reports have focused on Se volatilization from soils in laboratory incubation experiments39,40, with amendments of carbon and/or various Se species for enhancement of Se volatilization41,42. Temperature, Se concentration in soil, and the level of microbial biomass (especially in the rhizosphere) were among the most important environmental factors influencing Se volatilization43. These soil factors directly control microbial activity which influences the Se biomethylation and volatilization processes. Selenium volatilization rates vary enormously in the field due to these variables, with very high rates occurring spring and early summer44,45. For example, the mean rates were 150 and 25 μg Se/m2/day in February and October, respectively, in the San Francisco Bay, California, which is heavily contaminated by Se inflow from urban and industrial sources44. These factors such as temperature, soil moisture and organic C are quite different from southeast to northwest China, suggesting Se volatilization would be significant difference.

The majority of Se volatilization studies have focused on the Se volatilization in soils and sediments that were either naturally contaminated or amended with Se37,40,42. Few field studies have been conducted to investigate Se volatilization from natural environments31,46. The data available are too sparse to establish a reliable flux estimate to balance the assumed volatilization from land, limiting our ability to predict volatilized Se fluxes quantitatively. It was reported that the average volatile fluxes of Se in natural wetlands was 0.12 μg/m2/day (43.8 μg/m2/year). The flux rate of Se volatilization in upland (grassland) was estimated to be on the order of 100–200 μg/m2/year46,47. Given that most regions in China belong to upland soil, we postulate that all soils in humid and semi-humid environment volatilized Se at around this level (100–200 μg/m2/year) although many environmental variables (temperature, soil moisture, plant species, organic C levels, etc.) will cause fluctuations in actual Se volatilization.

Factors affecting Se volatilization and microbial biomass in soil

Volatilization of Se is a product of microbial activity in soil. Soil microorganisms play key roles in Earth’s biogeochemical cycles and global cycling of soil nutrients are strongly influenced by soil microbial communities. Sterilization of seleniferous soil by autoclaving completely eliminates Se volatilization4,48. Different environment (arid or humid) have different phenotypes of microorganisms, as well as varying populations and, consequently, different microbial activities. Soil microbial biomass and activity are primarily driven by moisture availability, soil nutrients such as nitrogen and organic carbon49 and vegetation cover50. It has been documented in many experiments that volatilization of Se can be enhanced by different organic amendments and also by many other environmental factors (e.g. soil moisture, soil management, etc.)35,36,37. Volatilization of sulfur, markedly similar to Se, was significant decreased by decreasing soil moisture51. Air-drying the soil severely inhibits Se volatilization52. Field studies have shown that Se emission rates were much lower at dry sites than in corresponding damp or wet conditions53. Global hotspots of abundances of soil microorganisms have been identified in tropical regions and the lowest soil microbial biomass was in arid and semi-arid regions49. In comparison with warm and wet tropical and subtropical climates in southeast China, soil microbial biomass would much less in cold and dry arid and semi-arid climate of northwest China. This strongly limits biogeochemical cycling of soil nutrients, including Se volatilization derived by soil microbes.

Volatilization of Se can be enhanced in the field with an available carbon source. Fierer et al.50 suggested that soil microbial biomass is strongly correlated to soil organic matter (SOM) content and plant productivity. The positive relationships were reported between soil microbial biomass and the contents of soil organic carbon50,54. The lowest contents of soil organic matter are in the northwest China (Fig. 3)55, which is considered to be one of the limiting resource for soil microorganisms.

Figure 3

Map of soil organic matter of China (Digital Soil Mapping from Institute of Agricultural Resources and Regional Planning, Chinese Academy of Agricultural Sciences,http://www.caas.ac.cn/datashare/spatialdata/om2ndse.jpg).

Temperature as one of the most important environmental factors influencing Se volatilization43, is another key factor limiting soil microbial population. Selenium volatilization is temperature-dependent and positively correlated with soil temperature56. In field measurements, volatilization of Se was reported to fluctuate seasonally, with greater rate in the spring and summer than that in the fall and winter, which correlated with soil temperature. The annual average temperature in northwest of China (<−5o C) is much low than in southeast regions (>15o C)57, which significantly repress the growth of soil microbes and Se volatilization. Poor plant cover is a factor affecting microbial abundance in northwest China as well. Soil from beneath plants generally have greater microbial population and diversity than soils associated with bare areas (Fuller, 1974), which tend to have greater microbial activity for Se volatilization. Furthermore, in dry environment, bioavailability of Se is less due to the lack of available moisture58. Poor plant productivity decrease microbial population, together with poor Se bioavailability of northwest China significantly limited Se volatilization. Moreover, soils in northwest China are saline and alkaline, which influences the availability of Se and limited Se volatilization by microorganisms.

Considering all these factors including low temperature, deposition, moisture availability and vegetation cover, all of which limited microbial biomass, abundances and activity, together with poor Se bioavailability in drier saline-alkaline soils. Selenium volatilization in northwest China would be much less or negligible, especially in the Gobi desert (bare land) (Fig. 4). In desertified and potential desertified lands less Se elevation (normal Se) were observed than Gobi desert (high Se) (Fig. 1A), because these lands were covered by steppe, more Se volatilization would be existed due to higher microorganisms and deposition (200 mm) than that in Gobi desert (<100 mm). It has been demonstrated that the soil microbial biomass carbon in the surface soil in Gobi deserts increased substantially with increasing mean annual deposition59,60, indicating higher microbial abundance in desertified and potential desertified lands than that in Gobi deserts. It is reasonable to believe that more Se would be volatilized from desertified and potential desertified lands than that in Gobi desert, causing relatively less Se accumulation in surface soil. In a word, high dry deposition from East Asian winter monsoon and negligible Se volatilization predominate the enrichment of Se in soil of Northwest China (Figs 4 and 5).

Figure 4: Schematic diagram of major factors and their potential impacts on soil Se volatilization in China, and the effects of volatilization and wet/dry deposition on the distribution of soil Se.

SOM refer to soil organic matter. The maps were created using Arc GIS Geographic Information Systems software version 10.2 (Environmental Systems Research Institute Inc, Redlands, Calif).

Figure 5: The fluxes of Se deposition and volatilization in three part of territory in China.

Southeast humid region (>800 mm); Central dry and humid region (400–800 mm); and Northwestern dry region (<400 mm). The maps were created using Arc GIS Geographic Information Systems software version 10.2 (Environmental Systems Research Institute Inc, Redlands, Calif).


We hypothesize that spatial variability of soil Se in China is potentially caused by balance between deposition (wet and dry) and volatilization mediated by microorganisms. Absolute accumulation rates were obtained by deducting Se volatilization from total deposition (Table 1).

In southeast China, high Se input occurred from deposition linked with East Asia summer monsoon, especially coastal area (200–400 μg/m2/yr). Although soil Se volatilization offset to some degree the Se increase in soil by deposition, high deposition rate substantially improve the Se contents in the soil (Fig. 5 and Table 1). In Central China the rate of Se deposition (40–160 μg/m2/yr) was roughly equal to the rate of soil Se volatilization (100–200 μg/m2/yr). Much less Se was accumulated in the soil and soil Se is near or a bit higher than that of the bedrock although Se input from monsoon-derived deposition has been for millions of years (Fig. 5). Probably this is the main cause for the formation of Se-poor belt in China. In northwest China it seemed that more Se was volatilized than deposited according to calculation if equal Se volatilization rate in southeast China exist (Table 1) and soil Se in this region should be decreased rather than increased. In fact, Se volatilization is negligible due to the much less microorganisms in dry soil.

In conclusion, we suggest that deposition associated with monsoons (wet and dry) and Se volatilization driven by biology, especially soil microorganisms are the key factors in controlling Se redistribution in terrestrial environments in other regions of the world. Future work should focus on a comprehensive quantification of Se distribution to refine our understanding of the roles of soil microbial communities and climate on Se redistribution and spatial variability not only in China but at the global scale; as such knowledge will provide predictions on Se distribution in arable soils, which will help to prevent health risks related to Se deficiency.


When calculating Se wet deposition, we assume that Se concentration in rainfall remains constant. In southeast and central China, wet deposition is the major contributor for soil Se and dry Se deposition is omitted due to unavailable data. In northwest China, dry deposition is the main contributor for surface soil Se and wet deposition is omitted due to much less rainfall. For calculation of Se volatilization, we assume that the rates of Se volatilization in southeast and central China are the same although some factors such as different climate and geology, might affect this value.

Additional Information

How to cite this article: Sun, G.-X. et al. Distribution of soil selenium in China is potentially controlled by deposition and volatilization?. Sci. Rep. 6, 20953; doi: 10.1038/srep20953 (2016).


  1. 1

    Rayman, M. P. Food-chain selenium and human health: emphasis on intake. Brit. J. Nutr. 100, 254–268 (2008).

    CAS  Article  Google Scholar 

  2. 2

    Zhu, Y. G. et al. Selenium in higher plants: understanding mechanisms for biofortification and phytoremediation. Trends Plant Sci. 14 (8), 436–442 (2009).

    CAS  Article  Google Scholar 

  3. 3

    Williams, P. N. Selenium characterization in the global rice supply chain. Environ. Sci. Technol. 43, 6024–6030 (2009).

    CAS  ADS  Article  Google Scholar 

  4. 4

    Sun, G. X., Liu, X., Williams, P. N. & Zhu, Y. G. Distribution and translocation of selenium from soil to grain and its speciation in paddy rice (Oryza sativa L.). Environ. Sci. Technol. 44, 6706–6711 (2010).

    CAS  ADS  Article  Google Scholar 

  5. 5

    Keshan disease and Kaschin-Beck disease (ed Tan, J. A. ) Ch. 3 and 4, 40–117 (Science Press, Beijing, China, 1989).

  6. 6

    Tan, J. A. & Huang, Y. J. Selenium in geo-ecosystem and its relations to endemic diseases in China. Water, Air, Soil Pollut. 57, 59–68 (1991).

    ADS  Article  Google Scholar 

  7. 7

    Gao, J. et al. Daily selenium intake in a moderate selenium deficiency area of Suzhou, China. Food Chem. 126, 1088–1093 (2011).

    CAS  Article  Google Scholar 

  8. 8

    Wang, Z. J. & Gao, Y. X. Biogeochemical cycling of selenium in Chinese environments. Appl. Geochem. 16, 1345–1351 (2001).

    CAS  Article  Google Scholar 

  9. 9

    Müller, A., Bertram, A. & Moschos, A. Seasonal and national differences in the selenium supply of horses across Europe. Tierarztl Prax Ausg G Grosstiere Nutztiere 40 (3), 157–166 (2012).

    Article  Google Scholar 

  10. 10

    Systra, Y. J. Bedrock and Quaternary sediment geochemistry and biodiversity in Eastern Fennoscandia and Estonia. - Forestry Studies Metsanduslikud Uurimused 53, 35–52 (2010).

    Article  Google Scholar 

  11. 11

    Lakin, H. W. Selenium in our environment. Trace Elements in the Environment, Adv. Chem. 123, Chapter 6, pp 96–111. (1973).

    CAS  Article  Google Scholar 

  12. 12

    Xia, W. P. & Tang, J. A. Comparative studies for selenium contents in Chinese rocks. Acta Scientiae Circumstantiae (Chinese) 10, 125–132 (1990).

    CAS  Google Scholar 

  13. 13

    Ross, H. B. An atmospheric selenium budget for the region 30° N to 90° N. Tellus B 37B, 78–90 (1985).

    CAS  ADS  Article  Google Scholar 

  14. 14

    Mosher, B. W. & Duce, R. A. A global atmospheric selenium budget. J. Geophys. Res. 92, 13289–13298 (1987).

    CAS  ADS  Article  Google Scholar 

  15. 15

    Nriagu, J. O. & Pacyna, J. M. Quantitative assessment of worldwide contamination of air, water, and soils by trace metals. Nature 333, 134–139 (1988).

    CAS  ADS  Article  Google Scholar 

  16. 16

    Nriagu, J. O. A global assessment of natural sources of atmospheric trace metals. Nature 338, 47–49 (1989).

    CAS  ADS  Article  Google Scholar 

  17. 17

    Wen, H. & Carignan, J. Ocean to continent transfer of atmospheric Se as revealed by epiphytic lichens. Environ. Pollut. 157, 2790–2797 (2009).

    CAS  Article  Google Scholar 

  18. 18

    Amouroux, D., Liss, P. S., Tessier, E., Hamren-Larsson, M. & Donard, O. F. X. Role of oceans as biogenic sources of selenium. Earth Planet. Sci. Lett. 189, 277–283 (2001).

    CAS  ADS  Article  Google Scholar 

  19. 19

    Blazina, T. et al. Terrestrial selenium distribution in China is potentially linked to monsoonal climate. Nat. Commun. 5, 4717 (2014).

    CAS  Article  Google Scholar 

  20. 20

    Qian, W. & Lin, X. Regional trends in recent precipitation indices in China. Meteorol. Atmos. Phys. 90, 193–207 (2005).

    ADS  Article  Google Scholar 

  21. 21

    Zhu, Q. F. & Tang, J. A., Selenium, iodine and fluorine in precipitation in China. Acta Scientiae Circumstantiae (Chinese) 8, 428–436 (1988).

    CAS  Google Scholar 

  22. 22

    Hashimoto, Y. & Winchester, J. W. Selenium in the atmosphere. Environ. Sci. Technol. 1 (4), 338–340 (1967).

    CAS  ADS  Article  Google Scholar 

  23. 23

    Cong, Z., Kang, S. C., Zhang, Y. L. & Li, X. D. Atmospheric wet deposition of trace elements to central Tibetan Plateau. Appl. Geochem. 25, 1415–1421 (2010).

    CAS  Article  Google Scholar 

  24. 24

    Amouroux, D. & Donard, O. F. X. Maritime emission of selenium to the atmosphere in eastern Mediterranean seas. Geophys. Res. Lett. 23 (14), 1777–1780 (1996).

    CAS  ADS  Article  Google Scholar 

  25. 25

    Wen, H. & Carignan, J. Reviews on atmospheric selenium: emissions, speciation and fate. Atmos. Environ. 41, 7151–7165 (2007).

    CAS  ADS  Article  Google Scholar 

  26. 26

    Lawrence, C. R. & Neff, J. C. The contemporary physical and chemical flux of aeolian dust: A synthesis of direct measurements of dust deposition. Chem. Geol. 267, 46–63 (2009).

    CAS  ADS  Article  Google Scholar 

  27. 27

    Zhang, X. Y. et al. Sources of Asian dust and role of climate change versus desertification in Asian dust emission. Geophys. Res. Lett. 30, ASC8.1–ASC8.4 (2003).

    Article  Google Scholar 

  28. 28

    Zhang, X. Y., Arimoto, R. & An, Z. S. Dust emission from Chinese desert sources linked to variations in atmospheric circulation. Atmospheres J. Geophys. Res. 102, D23, 28041–28047 (1997).

    ADS  Article  Google Scholar 

  29. 29

    Andreae, M. O. Climate effects of changing atmospheric aerosol levels. Vol. 16 (ed Henderson-sellers ) Ch. 10, 347–398 (Elsevier, Amsterdam, 1995).

  30. 30

    Duce, R. A. et al. The atmospheric input of trace species to the world ocean. Global Biogeochem. Cycles 5, 193–259 (1991).

    CAS  ADS  Article  Google Scholar 

  31. 31

    Vriens, B., Lenz, M., Charlet, L., Berg, M. & Winkel, L. H. Natural wetland emissions of methylated trace elements. Nat. Commun. 5, 3035 (2014).

    ADS  Article  Google Scholar 

  32. 32

    Ghauri, B. M. et al. Composition of aerosols and cloud water at a remote mountain site (2.8 kms) in Pakistan. Chemosphere: Global Science Change, 3 (1), 51–63 (2001).

    CAS  ADS  Google Scholar 

  33. 33

    Martens, D. & Suarez, D. Transformations of volatile methylated selenium in soil. Soil Biol. Biochem. 31, 1355–1361 (1999).

    CAS  Article  Google Scholar 

  34. 34

    Chau,Y. K., Wong, P. T. S., Silverberg, B. A., Luxon, P. L. & Bengert, G. A. Methylation of selenium in the aquatic environment. Science 192, 1130–1131 (1976).

    CAS  ADS  Article  Google Scholar 

  35. 35

    Zieve, R. & Peterson, P. J. Factors influencing the volatilization of selenium from soil. Sci. Total Environ. 19, 277–284 (1981).

    CAS  ADS  Article  Google Scholar 

  36. 36

    Frankenberger, Jr. W. T. & Karlson, U. Environmental factors affecting microbial production of dimethylselenide in a selenium-contaminated sediment. Soil Sci. Soc. Am. J. 53, 1435–1442 (1989).

    CAS  ADS  Article  Google Scholar 

  37. 37

    Abu-Erreish, G. M., Whitehead, E. I. & Olson, O. E. Evolution of volatile selenium from soils. Soil Sci. 106, 415–420 (1968).

    CAS  ADS  Article  Google Scholar 

  38. 38

    Doran, J. W. & Alexander, M. Microbial transformations of selenium. Appl. Environ. Microbiol. 33, 31–37 (1977).

    CAS  PubMed  PubMed Central  Google Scholar 

  39. 39

    Duckart, E. C., Waldron, L. J. & Donner, H. E. Selenium uptake and volatilization from plants growing in soil. Soil Sci. 153(2), 94–99 (1992).

    CAS  ADS  Article  Google Scholar 

  40. 40

    Stork, A., Jury, W. A. & Frankenberger, W. T. Accelerated volatilization rates of selenium from different soils. Biol. Trace Elem. Res. 69, 217–234 (1999).

    CAS  Article  Google Scholar 

  41. 41

    Wang, Z. J., Zhao, L. H. & Zhang, L. Effect of the chemical forms of selenium on its volatilization from soils in Chinese low selenium belt. J. Environ. Sci. 3 (2), 113–119 (1991).

    CAS  Google Scholar 

  42. 42

    Zieve, R. & Peterson, P. J. Volatilization of selenium from plants and soils. Sci. Total Environ. 32 (2), 197–202 (1984).

    CAS  ADS  Article  Google Scholar 

  43. 43

    Terry, N., Zayed, A. M., De Souza, M. P. & Tarun, A. S. Selenium in higher plants. Annu. Rev. Plant Physiol. Plant Mol. Boil. 51, 401–432 (2000).

    CAS  Article  Google Scholar 

  44. 44

    Hansen, D., Duda, P. J., Zayed, A. & Terry, N. Selenium removal by constructed wetlands: role of biological volatilization. Environ. Sci. Technol. 32 (5), 591–597 (1998).

    CAS  ADS  Article  Google Scholar 

  45. 45

    Lin, Z. Q. & Terry, N. Selenium removal by constructed wetlands: quantitative importance of biological volatilization in the treatment of selenium-laden agricultural drainage water. Environ. Sci. Technol., 37 (3), 606–615 (2003).

    CAS  ADS  Article  Google Scholar 

  46. 46

    Haygarth, P. M., Fowler, D., Sturup, S., Davison, B. M. & Tones, K. C. Determination of gaseous and particulate selenium over a rural grassland in the U.K. Atmos. Environ. 28 (22), 3655–3663 (1994).

    CAS  ADS  Article  Google Scholar 

  47. 47

    Barkes, L. & Fleming, R. W. Production of dimethylselenide gas from inorganic selenium by eleven soil fungi. Bull. Environ. Contam. Toxicol. 12 (3), 308–311 (1974).

    CAS  ADS  Article  Google Scholar 

  48. 48

    Doran, J. W. & Alexander, M. Microbial transformations of selenium. Appl. Environ. Microbiol. 33, 31–37 (1977).

    CAS  PubMed  PubMed Central  Google Scholar 

  49. 49

    Serna-Chavez, H. M., Fierer, N. & van Bodegom, P. M. Global drivers and patterns of microbial abundance in soil. Global Ecol. Biogeogr. 22 (10), 1162–1172 (2013).

    Article  Google Scholar 

  50. 50

    Fierer, N., Strickland, M. S., Liptzin, D., Bradford, M. A. & Cleveland, C. C. Global patterns in belowground communities. Ecol. Lett. 12, 1238–1249 (2009).

    Article  Google Scholar 

  51. 51

    Schoepfer, V. A., Bernhardt, E. S. & Burgin, A. J. Iron clad wetlands: Soil iron-sulfur buffering determines coastal wetland response to salt water incursion. J. Geophys. Res. Biogeosci. 119, 2209–2219 (2014).

    CAS  Article  Google Scholar 

  52. 52

    Cooke, T. D. & Bruland, K. W. Aquatic chemistry of selenium: evidence of biomethylation. Environ. Sci. Technol. 21 (12), 1214–1219 (1987).

    ADS  Article  Google Scholar 

  53. 53

    Francis, A. J., Duxbury, J. M. & Alexander, M. Evolution of dimethylselenide from soils. Appl. Environ. Microbiol. 28 (2), 248–250 (1974).

    CAS  Google Scholar 

  54. 54

    Cleveland, C. C. & Liptzin, D. C :N:P stoichiometry in soil: is there a ‘Redfield ratio’ for the microbial biomass? Biogeochemistry, 85, 235–252 (2007).

    Article  Google Scholar 

  55. 55

    Wu, H., Guo, Z. & Peng, C. Distribution and storage of soil organic carbon in China. Global Biogeochem. Cycles. 17 (2), 1048–1060 (2003).

    ADS  Google Scholar 

  56. 56

    Tan, J. A. Adsorption, volatilization, and speciation of selenium in different types of soils in China, (eds Frankenberger, W. T. Jr & Benson, S. L. ) Ch. 3, 43–68 (Marcel Dekker Inc, New York, 1994).

  57. 57

    Wang, J. X. L. & Gaffen, D. J. Late-twentieth-century climatology and trends of surface humidity and temperature in China. J. Climate 14, 2833–2845 (2001).

    ADS  Article  Google Scholar 

  58. 58

    Cowgill, U. M. Variations in annual precipitation and selenium accumulation by Milk-Vetch. J. Plant Nutr. 1 (1), 73–80 (1979).

    Article  Google Scholar 

  59. 59

    Li, X. Z. & Chen, Z. Z. Soil microbial biomass C and N along a climatic transect in the Mongolian steppe. Biol. Fertil. Soils 39, 344–351 (2004).

    Article  Google Scholar 

  60. 60

    Wang, Y. M., Wang, J. H., Qi, Y. & Yan, C. Z. The map of desert distribution in 1:100,000 in China. Cold and Arid Regions Science Data Center at Lanzhou, (2005).

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This project was financially supported by the Natural Science Foundation of China (No. 41371459), the State Key Program of Natural Science Foundation of China (No. 41430858, 41330853) and the National High Technology Research and Development Program of China (863 Program, 2013AA06A209).

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G.X.S., A.A.M., G.L. and Y.G.Z. wrote the main text, Z.C., L.Y. and S.C.C., prepared figures. G.L. and Z.C. contributed to the development of specific aspects of the proposed hypotheses. All authors reviewed the manuscript.

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Correspondence to Yong-Guan Zhu.

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Sun, G., Meharg, A., Li, G. et al. Distribution of soil selenium in China is potentially controlled by deposition and volatilization?. Sci Rep 6, 20953 (2016). https://doi.org/10.1038/srep20953

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