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. 2016 Mar 21;6:23332. doi: 10.1038/srep23332

Historical Records of Mercury Stable Isotopes in Sediments of Tibetan Lakes

Runsheng Yin 1,2, Xinbin Feng 1,a, James P Hurley 2,3,4, David P Krabbenhoft 5, Ryan F Lepak 2, Shichang Kang 6,7, Handong Yang 8, Xiangdong Li 9
PMCID: PMC4800404  PMID: 26996936

Abstract

The Tibetan Plateau (TP), known as the “Third Pole”, is a critical zone for atmospheric mercury (Hg) deposition. Increasing anthropogenic activities in the globe leads to environmental changes, which may affect the loading, transport and deposition of Hg in the environment. However, the deposition history and geochemical cycling of Hg in the TP is still uncertain. Our records of Hg and Hg isotopes in sediment profiles of the two largest lakes in the TP, Lake Qinghai and Nam Co, show increased Hg influx since last century, with the maximum Hg influx enrichment ratios of 5.4 and 3.5 in Lake Qinghai and Nam Co, respectively. Shifts in negative δ 202Hg in Lake Qinghai (−4.55 to −3.15‰) and Nam Co (−5.04 to −2.16‰) indicate increased atmospheric Hg deposition through rainfall, vegetation and runoff of soils. Mass independent fractionation of both even-Hg (∆ 200Hg: +0.05 to +0.10‰) and odd-Hg (∆ 199Hg: +0.12 to +0.31‰) isotopes were observed. Positive Δ 200Hg suggest high proportion of precipitation-derived Hg in the TP, whereas the positive Δ 199Hg results from Hg(II) photo-reduction. Both lakes show increasing Δ 199Hg since the 1900 s, and we conclude that with the decrease of ice duration, Hg(II) photo-reduction may have been accelerated in these TP lakes.

The Tibetan Plateau (TP), with an area of ~2.5 × 106 km2 and an average elevation of >4000 m above sea level, covers ~26% of land and <1% of population in China. Due to remote location and low population density, the TP is minimally impacted by local anthropogenic activities. However, increasing global industrialization has accelerated the loading, transport and deposition of volatile pollutants (e.g., persistent organic pollutants) to the TP1. Like persistent organic pollutants, mercury (Hg) is a globally distributed semi-volatile pollutant and exhibits similar patterns of cycling in the atmosphere2, with growing evidence that alpine regions act as intensive sinks of atmospheric Hg2,3. High atmospheric Hg deposition rates and elevated Hg levels in snow have been reported in the TP4,5. China and India are two of the largest anthropogenic Hg emission countries to the TP and other sites of the world6. Mercury deposited to the watershed and lakes is susceptible to methylation to the bioaccumulable neurotoxin, methylmercury (MeHg)7. High levels of MeHg in various aquatic species in TP lakes have been shown, indicating high environmental risks of Hg in this region7.

Global industrialization not only cause increasing Hg deposition, but also result in environmental changes. Mercury is a redox-sensitive metal, and its biogeochemical cycling is particularly susceptible to environmental changes8,9,10,11. Growing evidence suggests that montane regions experience more rapid environmental changes than lower elevations12. For instance, the TP has warmed over the past several decades at twice the global average rate13. This has resulted other dependent changes such as cryospheric systems and hydrological regimes12,13,14, which are particularly important to Hg biogeochemical cycling because aquatic environments are active sites of Hg methylation and bioaccumulation7,8,9,10,11.

Mercury has seven natural stable isotopes (196, 198, 199, 200, 201, 202 and 204), and our understanding of environmental fate of Hg has been enhanced by recent application of Hg isotope geochemistry. In the environment, Hg can undergo both mass dependent fractionation (MDF) and mass independent fractionation (MIF). MDF occurs during a variety of chemical, physical, and biological processes, and has been used to better understand the processes controlling Hg transport, transformation and bioaccumulation15,16. MIF signatures can provide a unique fingerprint of specific chemical pathways, such as photochemical reactions17,18. Large variations of both Hg-MDF and -MIF signatures have been documented in different environmental compartments16, and can provide multi-dimensional information to identify the sources and better understand biogeochemical Hg cycling15.

Sediment profiles coupled with high resolution dating (e.g., 210Pb and 137Cs) have been broadly used to evaluate historical changes of Hg deposition rate5. As the “water tower of Asia”, the TP provides an ideal site to reconstruct environmental changes due to its sensitivity to environmental change and the lack of local pollution sources13,14. In this study, sediment profiles collected from two of the largest lakes in the TP (Lake Qinghai and Nam Co) were age-dated and analyzed for total Hg concentration (THg) and Hg isotopic composition. The objectives of this study were (1) to elucidate the history of Hg influx and source changes in the TP, and (2) to investigate the influence of global change on the biogeochemical cycle of Hg in this fragile alpine ecosystem.

Experimental section

Study area and sampling

Lake Qinghai (3194 m), the largest lake (4382 km2) in the TP, is located in the northeast of the plateau. Nam Co (4730 m), the second largest lake (1920 km2) in the TP, is centrally located (Fig. 1). Lake Qinghai is fed from a catchment of ~29,660 km2, and Nam Co has a catchment area of ~15,000 km2. The mean annual precipitations in Lake Qinghai and Nam Co are 357 and 414 mm19,20,21,22. The present day climate in both lakes is influenced by the Asian monsoon with dry winters, and precipitation mainly occurring in the summer season. The glaciated area of the catchment of Lake Qinghai and Nam Co is ~10 km2 and 197 km2, respectively, accounting for 0.03% and 1.31% of the catchment. Hence, hydrologic sources to both lakes mainly consist of precipitation, not glacial melt14.

Figure 1. Study area and sampling sites.

Figure 1

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(This image is modified by R-S Yin, on basis of the a Wikimedia Commons map: https://commons.wikimedia.org/wiki/File:Topografic_map_of_Tibetan_Plateau.png#filelinks).

Sediment cores were taken from the deepest regions of Lake Qinghai (depth: 25.3 m) in 2006 and Nam Co (depth: ~60 m) in 2009 using HTH gravity corers. The Lake Qinghai core was sectioned in the field using a stainless steel slicer at 0.5 cm intervals from the surface to 5 cm, and then at 1.0 cm intervals to the base of the core. The Nam Co core (21 cm) was sectioned using a stainless steel slicer at 0.5 cm intervals from the surface to the base of the core. Samples were freeze-dried and homogenized prior to 210Pb dating, total organic contents (TOC), THg and Hg isotope measurements. Sedimentation rate and TOC methodologies have been reported by Lami et al.20 and Li et al.22.

Hg concentration analysis

THg in sediments was analyzed by direct combustion and atomic absorbance detection based on Lepak et al.23 at the USGS Wisconsin Mercury Research Lab. SRM (IAEA SL 1) recoveries were within 90~110%, and coefficients of variation of triplicate analyses were less than 10%.

Mercury isotopic composition analysis

Based on the measured THg concentration [Table S1 of Supplementary Information (SI)], samples and certified reference materials (NIST 2711 and MESS-2) were digested and diluted prior to isotopic measurement on a Neptune Plus MC-ICP-MS housed at the University of Wisconsin-Madison’s State Laboratory of Hygiene. A more detailed method description for MC-ICP-MS analyses is given in the SI. Following the convention recommended by Blum and Bergquist24, Hg-MDF is expressed in δ 202Hg notation in units of permil (%), referenced to the NIST-3133 Hg standard (analyzed before and after each sample):

graphic file with name srep23332-m1.jpg

Hg-MIF is reported in Δ notation (Δ xxxHg) and describes the deviation from mass dependency in units of permil (‰). MIF is the difference between the measured δ xxxHg and the theoretically predicted δ xxxHg value using the following formula24.

graphic file with name srep23332-m2.jpg

where β is the independent isotope-specific scaling factor determined by the laws of MDF, which 0.2520 for 199Hg, 0.5024 for 200Hg, and 0.7520 for 201Hg.

UM-Almadén solutions23 were also measured as 10% of the samples. Data uncertainty reported in this study reflects the larger value of either the external precision of replication of UM-Almadén or the measurement uncertainty of standard reference materials. The overall average and uncertainty of all UM-Almadén measurements (δ 202Hg: −0.50 ± 0.04‰; Δ 199Hg: −0.03 ± 0.03‰; Δ 200Hg: +0.02 ± 0.03‰, σ, n = 9) agreed well with previous results23. Measurements of replicate digests of NIST 2711 (δ 202Hg: −0.21 ± 0.05%; Δ 199Hg: −0.17 ± 0.03%; Δ 200Hg: +0.01 ± 0.03‰, σ, n = 3) and MESS-1 (δ 202Hg −1.95 ± 0.05‰; Δ 199Hg +0.01 ± 0.03‰; Δ 200Hg: +0.04 ± 0.03‰, σ, n = 3) were also comparable with previous studies23,25,26,27.

Results and Discussion

Mercury concentration profiles

Historical sediment profiles from both Lake Qinghai and Nam Co show a general trend of increasing THg over the past century (Fig. 2A). THg in sediment provides insight into pollution status, however, influx rates of Hg (sedimentation rate × THg) provide the best estimates of inputs of Hg to lake (Fig. 2B). Preindustrial influxes of Hg in Lake Qinghai and Nam Co are about 3.1 and 5.7 ng cm−2 yr−1, respectively, with the highest Hg influxes in Lake Qinghai and Nam Co at 16.5 and 20.3 ng cm−2 yr−1. Mercury influxes among remote lakes have shown to be positively correlated to ratios of terrestrial catchment area (AC) to lake area (AL)28. Nam Co has an AC/AL of 7.8 higher than Lake Qinghai (AC/AL = 6.7). Mercury influx profile shifts are more clearly evident by calculating influx ratios (influxsample/influxbackground, influxes of each sediment with respect to the geochemical background) (Fig. 2C). Influxsample and influxbackground were the Hg influx of a given sample and the deepest sediment sample in each core, respectively. The maximum influx ratios of Hg in the 21st century are about 5.4 in Lake Qinghai and 3.5 in Nam Co, consistent with other studies of remote lake sediment cores, where Hg influxes have increased by a factor of 3 to 5 compared to the pre-industrial values5,29. Both profiles indicate increased Hg deposition starting from the early 1900 s, with especially intensive increases since the 1960 s (Fig. 2 A–C). This is in agreement with the increased enhanced global Hg emission (especially China and India) and atmospheric Hg concentrations during the last few decades5.

Figure 2.

Figure 2

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Sediment profiles of THg (A), Hg influx (B), Hg influx ratio (C), global average temperature anomaly ((D) according to Hansen et al.30) and temperature in TP ((E), according to Zhang et al.13), TOC ((F) according to Lami et al.20 and Li et al.22), δ 202Hg (G), ∆ 200Hg (H), ∆ 199Hg (I) and ice duration ((J) according to Che et al.19 and Ke et al.21) in Lake Qinghai and Nam Co.

The increase of Hg influx in Lake Qinghai and Nam Co is also likely synchronous with the rising global temperature, which starts in the early 1900 s, and has accelerated since the 1960 s (Fig. 2D)30. Temperature increase in the TP is twice as high as the global average from 1957 to 2012 (0.036 ± 0.003 °C yr−1) (Fig. 2E). This has not only caused increased precipitation at an average annual rate of 10.9 mm per decade from 1961 to 2008, but also resulted in continuous increases of growing season (~1.04 day y−1)31 and vegetation coverage (3 961.9 km−2 yr−1)32 during the past 2 to 3 decades. Precipitation and vegetation (litterfall) are efficiently scavengers of atmospheric Hg2,4. Increased precipitation have also caused lake expansion and enhanced soil erosion in the TP14. For instance, Nam Co expanded by 20.2% in area between 1976 and 2010, and an average depth increase of 0.11 m−1 yr−1 was observed in Lake Qinghai in recent years14. Enhanced soil erosion in Lake Qinghai and Nam Co during the past few decades has been verified by inert tracers (such as Ti, Ni, Al, Fe, etc)33,34,35. Precipitation and vegetation (litterfall) are important inputs of Hg to pristine soils. The TP is mostly covered by typical alpine meadow and steppe31. Increase of plant production in the TP resulted in the increase of soil organic carbon density (0.1 g C m−2 yr−1) during 1981 to 201036. Organic matter has a strong affinity for Hg37. Runoff of organic soil particles may effectively capture vegetation and precipitation-derived Hg from soils and the water column, and ultimately sequester it into sediments37,38. A recent study observed that organic matter (OM), in sediments of Lake Qinghai is primarily (80%) of terrestrial origin39. Significant linear correlations between THg and TOC (P < 0.01, ANOVA test) were observed in Lake Qinghai and Nam Co (Fig. 3). Overall, we suggest that increased anthropogenic Hg emission, enhanced atmospheric Hg deposition (through precipitation and vegetation) and soil erosion, may result in the increased Hg accumulation in the TP lakes.

Figure 3. Correlations between THg and TOC in sediments of Lake Qinghai and Nam Co.

Figure 3

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Mass dependent fractionation of mercury isotopes

Sediments from Lakes Qinghai and Nam Co showed highly variable δ 202Hg values, ranging from −4.55 to −3.15‰ and from −5.04 to −2.16‰, respectively (Fig. 2G), which are much lower than previously reported data for industrial point Hg sources16,25,26,27,40,41,42,43,44,45 (δ 202Hg: −1.5 to 0‰), consistent with the fact that Lakes Qinghai and Nam Co are less impact by local point sources. Our data are more similar to sediments collected from pristine regions (δ 202Hg: −2 to −3‰)42,45, which mainly receive Hg from atmospheric deposition. Previous studies have reported much higher δ 202Hg (0 to +1.0‰) in Hg0g collected from pristine sites46 in comparison with that collected from urban-industrial regions (δ 202Hg: −3 to −0‰)47,48,49. This indicates that Hg with lower δ 202Hg values may be preferentially removed during long range transport and deposition through precipitation and litterfall. Indeed, precipitations in Northern America have shown more negative δ 202Hg (−4 to 0‰) than that of Hg0g (δ 202Hg: −0.5 to +1.0‰) in the same areas46,49,50,51. For instance, precipitations from urban-industrial regions have shown highly negative δ 202Hg values of down to −4.27‰ in China52 and −4.37‰ in Florida50, being similar to our data of TP sediments. Due to close to China and India, it is possible for such highly fractionated rain contributions to the TP. However, our knowledge about the Hg isotope signatures in precipitation of the TP is limited to one single precipitation event, representing large variabilities53. Previous studies also reported negative δ 202Hg of −4 to −1‰ for plants, demonstrating that lighter Hg isotopes are preferentially binding within the foliage46,47,54. Increased atmospheric Hg deposition through rainfall and litterfall have caused soils in montane regions to have much negative δ 202Hg values2. Our observation of negative δ 202Hg values is consistent with the fact that atmospheric deposition is the main input of Hg to Lake Qinghai and Nam Co5.

In addition to the source effect, post-depositional processes in the water column may also affect δ 202Hg in sediments. Mercury deposited into lakes can be re-emitted to the atmosphere, while the remaining fraction is adsorbed on and settled by sediment particulate. The product Hg(0) during volatilization, microbial reduction and photoreduction processes could result in more negative δ 202Hg values and, likewise, the residual Hg in the water column will result in a more positive δ 202Hg values17,18,55,56,57. Adsorption of aqueous Hg(II) by sediment particles containing thiol groups58, goethite59 and sulfides60 is likely cause negative shifts of δ 202Hg (−0.60‰) in the solid phase. However, significant shift of δ 202Hg may only occur when very small fraction of Hg is adsorbed relative to the total Hg in a system. Given the fact that particulate Hg is the dominate form of total Hg in Nam Co (86.7%) and other TP lakes61,62, we would not expect a significant negative shift of δ 202Hg during adsorption of aqueous Hg(II) by sediments.

Like the THg profiles, δ 202Hg generally increases from the deep part to the surface layer of the two cores (Fig. 2G). This pattern is similar to sediment cores collected near anthropogenic Hg point sources, where increased inputs of anthropogenic Hg with δ 202Hg ranges from −1 to 0‰ have shown in upper layer sediments25,43,44. It is unclear whether the increase of δ 202Hg in this study is the result of global anthropogenic Hg input, however, due to the sparse population and industrial activities within the TP, local point sources may not explain the significant δ 202Hg increase upcore. The shift of δ 202Hg may be explained by a combined effect of enhanced precipitation, net primary production and soil erosion, all of which could incorporate more isotopic heavier Hg0g into waters, soils and sediments. Significant correlations between δ 202Hg and THg with TOC were observed in Nam Co (P < 0.01, ANOVA test), when compared to that in Lake Qinghai (Fig. 4A,B). This suggests that the shifts of δ 202Hg in Nam Co are more influenced by input of precipitation and vegetation derived Hg, and runoff of organic soils, as supported by the smaller lake area (1920 km2) of Nam Co. The lower correlation between δ 202Hg and THg (P > 0.05) with TOC (P > 0.05) in Lake Qinghai may indicate sediments more influenced by lake processes, with a the much large lake area (4382 km2).

Figure 4.

Figure 4

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Relations of δ 202Hg to THg (A) and TOC (B) in sediments of Lake Qinghai and Nam Co.

Mass independent fractionation of 200Hg

In this study, small but detectable MIF of 200Hg was found in Lake Qinghai (∆ 200Hg: +0.07 to +0.10‰) and Nam Co (∆ 200Hg: +0.05 to +0.08‰) (Fig. 2H). When compared to the analytical uncertainty for ∆ 200Hg (±0.03‰), these results are considered significant. ∆ 200Hg values of sediments from both Lake Qinghai and Nam Co were also significantly higher (P < 0.01, T-test) than UM-Almadén. The mechanism for MIF of 200Hg is still unclear; however, prior studies have suggested that 200Hg MIF is likely linked to photo-initiated Hg0g oxidation49,51. Significant 200Hg MIF has been reported in atmospheric Hg samples46,48,49,50,51,. In general, Hg0g is characterized by negative ∆ 200Hg (−0.4 to 0‰), whereas precipitation (containing oxidized Hg species) is characterized by positive ∆ 200Hg (+1.2 to 0‰)46,48,49,50,51. Industrial Hg has shown to be absent of 200Hg MIF (∆ 200Hg: ~0‰)16,26,27,40. MIF of 200Hg has not been reported in soils and sediments from urban-industrial regions41,42,43,44,45, most likely a result of the dilution effect by industrial Hg. However, vegetation can incorporate atmospheric Hg0g, and therefore have shown slightly negative ∆ 200Hg (mean: −0.10‰, n = 5) in Northern Sweden forests54. A recent study also reported pronounced positive ∆ 200Hg in sediments collected from the Laurentian Great Lakes where precipitation is the major Hg input to sediments23. Our observation of positive ∆ 200Hg may highlight the importance of precipitation Hg in TP lakes.

If precipitation ∆ 200Hg signature did not change over time in the TP, increases of ∆ 200Hg in sediment profiles result from enhanced precipitation Hg inputs are expected. However, we observed the consistent ∆ 200Hg pattern in both Lake Qinghai and Nam Co (Fig. 2H). The lack of increased ∆ 200Hg with elevated precipitation rates in this study may be explained by the isotope dilution of ∆ 200Hg by other sources. The magnitude of ∆ 200Hg in precipitation have shown to decrease from pristine to urban-industrial regions49,50,51, suggesting the dilution by industrial Hg (∆ 200Hg: ~0‰)16,26,27,40. As mentioned earlier, enhanced input of soil- and vegetation-derived Hg with negative to zero ∆ 200Hg, may also lessen the increase of ∆ 200Hg in sediments. However, due to the lack of Hg isotope data in precipitation and soils throughout time, assessment of Hg contributions from precipitation and soil erosion was not performed in our study.

Mass independent fractionation of 199Hg and 201Hg

Positive MIF of odd Hg isotopes (199Hg and 201Hg) was observed in sediment of both lakes (Fig. 2I). The ∆ 199Hg values in Lake Qinghai and Nam Co range from +0.19 to +0.31‰ and +0.12 to +0.28‰, respectively. There are two known possible mechanisms for odd-MIF: the nuclear volume effect (NVE)63 and the magnetic isotope effect (MIE)17. Laboratory experiments demonstrated that NVE can be caused during elemental Hg0 volatilization64, equilibrium Hg-thiol complexation58 and dark Hg(II) reduction57 with ∆ 199Hg/∆ 201Hg of ~1.6. Effects on MIE are mainly due to the photoreactions of aqueous Hg species in the presence of dissolved organic carbon (DOC), resulting in ∆ 199Hg/∆ 201Hg of 1.00~1.3017,18. This is comparable with the observed ∆ 199Hg/∆ 201Hg ratio (1.07 ± 0.07, 2σ) in all sediments investigated in this study, suggesting that aqueous Hg(II) photo-reduction is the possible process to cause MIF of Hg isotopes (Fig. 5).

Figure 5. Relations between ∆ 199Hg and ∆ 201Hg in sediments of Lake Qinghai and Nam Co.

Figure 5

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The positive ∆ 199Hg in TP lake sediments is different from previous data on sediments collected from industrial-urban regions, which mainly have negative to zero ∆ 199Hg27,41,43,44,45. Industrial Hg sources have shown average ∆ 199Hg close to zero16,40,41,43, and continental soils and vegetation mainly showed negative ∆ 199Hg values (−0.5 to 0‰)2,26,46,47,54. The positive ∆ 199Hg of the TP sediments may be explained by the inputs of Hg with positive ∆ 199Hg or Hg(II) photoreduction in the water column, or both. Positive ∆ 199Hg values (0 to +1.0‰) have been reported for precipitation collected from different sites of the world49,50,51,52,53. Interestingly, sediment cores in this study reflect a shift of +0.1‰ in Δ 199Hg values since the early 1900 s (Fig. 2I), three times higher than our analytical uncertainty for UM-Almadén (Δ 199Hg: ±0.03‰, σ). Increased precipitation tends to cause rise of ∆ 199Hg in sediments, however, it also results in more input of vegetation- and soil-derived Hg (with negative ∆ 199Hg) to lakes, likely to lessen the increase of ∆ 199Hg in sediment profiles. Like the consistent ∆ 200Hg profiles, we would not expect a significant shift of ∆ 199Hg due to enhanced inputs of vegetation- and soil-derived Hg.

In this study, increases of Δ 199Hg are more likely the result from enhanced Hg(II) photoreduction in the lake water column before incorporation into sediments. Photoreduction of Hg is largely controlled by solar irradiation and water conditions17,18,42,65. Long-term observation demonstrated no clear patterns on solar irradiation in the TP66. The increased Δ 199Hg patterns in both lakes (Fig. 2I) show similar patterns with temperature rising (Fig. 2D,E). Positive relations between Δ 199Hg and rising temperatures were observed (Fig. S1 of SI). Temperature rising have caused decreases of ice cover in the TP lakes, which can lead to greater exposure to sunlight for increased photochemical activity9,10. Ice cover should play an important role in controlling Hg(II) photoreduction in the TP lakes, considering the long-term of the ice duration in the TP lakes. Due to rising temperature, ice duration in the TP lakes have declined (Fig. 2J). Negative linear correlations between temperature and time of ice duration in 36 lakes in the TP has been also observed13. We speculate that the thickness of the lake ice would also decline along with rising temperatures, causing more water to be exposed to sunlight.

Positive relationships between ∆ 199Hg and δ 202Hg (Fig. 6A) were observed in Lake Qinghai (P < 0.01) and Nam Co (P < 0.01). Laboratory experiments on Hg(II) photoreduction also revealed positive relations between ∆ 199Hg and δ 202Hg with a δ 202Hg/∆ 199Hg of 0.8316, which is much smaller than that observed for Lake Qinghai (δ 202Hg/∆ 199Hg = 8.88) and Nam Co (δ 202Hg/∆ 199Hg = 5.75). This suggests that Hg(II) photoreduction may not be the main cause of the positive shifts of δ 202Hg in the TP lakes. The positive relations between ∆ 199Hg and δ 202Hg indicate that enhanced Hg(II) photoreduction and δ 202Hg shifts are induced by similar reasons, possibly due to the temperature effect. Indeed, warming not only causes decrease of ice duration which leads to higher Hg(II) photoreduction, but also results in higher influxes of atmospheric Hg (with higher δ 202Hg values) though rainfall and soil erosion into the lakes. Our assumption has been supported by significant positive relations between ∆ 199Hg and THg (P < 0.01) (Fig. 6B), and TOC (P < 0.01) (Fig. 6C) in Nam Co. Like δ 202Hg, we also observed less correlation between ∆ 199Hg and THg (P > 0.05), and TOC (P > 0.05) in Lake Qinghai, which indicates that Lake Qinghai may be more influenced by in-lake processes. Further research on water column Hg processes of Lake Qinghai are needed to better understand the variations of Hg isotopes in this study.

Figure 6.

Figure 6

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Relations of ∆ 199Hg to δ 202Hg(A), THg (B) and TOC (C) in sediments of Lake Qinghai and Nam Co.

Environmental implications

Alpine regions function as important convergence zones for atmospheric Hg, and have a rapid response to environmental change. Environmental changes such as enhanced precipitation, higher terrestrial plant biomass, and erosion of soils, may result in greater atmospheric Hg deposition and transport of historically deposited legacy Hg into the lakes of the in the TP. Dramatic lake ice cover reduction in TP may lead to increased Hg(II) photoreduction and evasion of Hg0(g). The results of this study suggest that environmental change signals can be seen in the Hg isotopic distribution in the TP lake sediments. It should be mentioned that increased precipitation and glacier shrink have resulted in lake expansion and flooding of organic soil horizons67, which may affect the food web structures, Hg methylation and demethylation rates, and Hg fluxes on sediment-water–atmosphere interfaces of the TP lakes. Further studies are therefore needed.

Additional Information

How to cite this article: Yin, R. et al. Historical Records of Mercury Stable Isotopes in Sediments of Tibetan Lakes. Sci. Rep. 6, 23332; doi: 10.1038/srep23332 (2016).

Supplementary Material

Supplementary Information
srep23332-s1.doc (191KB, doc)

Acknowledgments

This study was supported by China Basic Research Program (973 Project 2013CB430000) and the Natural Science Foundation of China (41303014, 41173024). We acknowledge the help of Dr. S. Turner at University College London and Dr. G. J. Wu at Institute of Tibetan Plateau Research in the field work, and acknowledge funding from The Leverhulme Trust for support of the field work and the project (Project F/07 134BF). Three anonymous reviewers are acknowledged for their thoughtful comments.

Footnotes

Author Contributions R.Y., X.F., J.P.H., D.P.K., S.C.K. and H.D.Y. conceived the project. S.C.K. and H.D.Y. provided the samples. R.Y. and R.F.L. measured the Hg isotopic compositions. R.Y., X.F., J.P.H., R.F.L., D.P.K., S.C.K., H.D.Y. and X.D.L. interpreted the data. R.Y. and J.P.H. prepared the manuscript with review comments from other authors.

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