Hostname: page-component-cd9895bd7-dzt6s Total loading time: 0 Render date: 2024-12-21T00:12:45.320Z Has data issue: false hasContentIssue false
  • English
  • Français

210 Pb dating of the Miaoergou ice core from the eastern Tien Shan, China

Published online by Cambridge University Press:  26 July 2017

Chaomin Wang ,
Shugui Hou ,
Hongxi Pang ,
Yaping Liu ,
Heinz W. Gäggeler ,
Leonhard Tobler ,
Sönke Szidat  and
Edith Vogel
Chaomin Wang
Affiliation:
School of Geographic and Oceanographic Sciences, Nanjing University, Nanjing, China E-mail: shugui@nju.edu.cn
Shugui Hou
Affiliation:
School of Geographic and Oceanographic Sciences, Nanjing University, Nanjing, China E-mail: shugui@nju.edu.cn
Hongxi Pang
Affiliation:
School of Geographic and Oceanographic Sciences, Nanjing University, Nanjing, China E-mail: shugui@nju.edu.cn
Yaping Liu
Affiliation:
State Key Laboratory of Cryospheric Science, Cold and Arid Regions Environmental and Engineering Research Institute, Chinese Academy of Sciences, Lanzhou, China
Heinz W. Gäggeler
Affiliation:
Labor für Radio-und Umweltchemie, Paul Scherrer Institut, Villigen PSI, Switzerland
Leonhard Tobler
Affiliation:
Labor für Radio-und Umweltchemie, Paul Scherrer Institut, Villigen PSI, Switzerland
Sönke Szidat
Affiliation:
Laboratory for Radio and Environmental Chemistry, University of Bern, Bern, Switzerland
Edith Vogel
Affiliation:
Laboratory for Radio and Environmental Chemistry, University of Bern, Bern, Switzerland
Rights & Permissions [Opens in a new window]

Abstract

In 2005, two ice cores with lengths of 58.7 and 57.6 m respectively to bedrock were recovered from the Miaoergou flat-topped glacier (43°03′19″ N, 94°19′21″ E; 4512 m a.s.l.), eastern Tien Shan. 210Pb dating of one of the ice cores (57.6 m) was performed, and an age of AD 1851 ± 6 at a depth of 35.2 mw.e. was determined. For the period AD 1851-2005, a mean annual net accumulation of 229 ± 7 mm w.e. a–1 was calculated. At the nearby oasis city of Hami (~80 km from the Miaoergou flat-topped glacier) the annual precipitation rate is 38 mm w.e. a–1, hence glacial meltwater is a major water supply for local residents. The surface activity concentration of 210Pbex was found to be ~400 mBq kg–1, which is higher than observed at other continental sites such as Belukha, Russia, and Tsambagarav, Mongolia, which have surface activity concentrations of 280 mBq kg–1. The 210Pb dating agrees well with the chronological sequence deduced from the annual-layer counting resulting from the seasonalities of d18O and trace metals for the period AD 1953-2005, and ^-activity horizons resulting from atmospheric nuclear testing during the period AD 1962-63. We conclude that 210Pb analysis is a suitable method for obtaining a continuous dating of the Miaoergou ice core for ~160 years, which can also be applied to other ice cores recovered from the mountains of western China.

Keywords

accumulationglacier chemistryice chronology/datingice core
Type
Research Article
Information
Annals of Glaciology , Volume 55 , Issue 66 , 2014 , pp. 105 - 110
Copyright
Copyright © The Author(s) [year] 2014

Introduction

Mid- or low-latitude glaciers represent a natural archive, well suited for studying past environmental and climatic conditions (Reference Hou, Qin, Zhang, Kang, Mayewski and WakeHou and others, 2003; Reference Kang, Mayewski, Yan and QinKang and others, 2003; Reference BarbanteBarbante and others, 2004; Reference Yang and Yao Tand WangYang and others, 2006; Reference Wang, Gong, Zhang and YaoWang and others, 2010; Reference XuXu and others, 2010; Reference ShenShen and others, 2012; Reference WuWu and others, 2013). Accurate dating is an essential prerequisite for the correct interpretation of paleoclimatic information from ice-core records. For the time period covered by ice cores, ranging from decades to thousands of years, many different ice-core dating methods have been used, including profile characteristics (e.g. seasonal variation of particles; conductivity characteristics; stable isotopes and major ions contained in the core) (Reference Oeschger and LangwayOeschger and Langway, 1989; Reference AlleyAlley and others, 1997; Reference PetitPetit and others, 1999; EPICA Community Members, 2004; NorthGRIP Members, 2004; Reference SvenssonSvensson and others, 2005). The assignment of reference layers to known sources (β-activity peak from nuclear bomb debris, volcanic ash horizons, etc.) (Reference Legrand and DelmasLegrand and Delmas, 1987; Reference Cole-Dai, Mosley-Thompson, Wight and ThompsonCole-Dai and others, 2000), as well as radioisotope dating and glacier flow models, have also been used (Reference Johnsen, Dansgaard, Clausen and LangwayJohnsen and others, 1972; Reference Raisbeck and YiouRaisbeck and Yiou, 1985; Reference Raisbeck, Yiou, Bourles, Lorius, Jouzel and BarkovRaisbeck and others, 1987; Reference Ciais, Jouzel, Petit, Lipenkov and WhiteCiais and others, 1994). More than 20 dating indicators have been applied to the Greenland ice sheet GISP2 and GRIP ice cores (Reference DansgaardDansgaard and others, 1993; Reference MeeseMeese and others, 1997). The choice of the most appropriate dating method depends on the timescale and accuracy requirements. Multi-proxy annual-layer counting is the most accurate dating method (Reference AlleyAlley and others, 1997). Reference horizons are usually used to verify and cross-check the annual-layer counting dating (Reference Pourchet, Pinglot and LoriusPourchet and others, 1983; Reference EichlerEichler and others, 2000; Reference Liu, Hou, Hong, Soon, Lee and WangLiu and others, 2011).

The time range accessible using radioactive isotope 210Pb dating is ~150 years and is determined by the 22.3 year half-life of 210Pb, a product of the natural 238U decay series (Reference Gäggeler, Von Gunten, Rössler, Oeschger and SchottererGäggeler and others, 1983; Knusel and others 2003; Reference OlivierOlivier and others, 2003). 238U is the most abundant isotope of uranium, a primordial radioactive element in nature. 238U is ubiquitous in nature at an average level of ~5 ppm in soil. The half-life of 238U is 4.6 x 109 years. 238U decays after several intermediate nuclides into 222Rn which has a half-life of 3.8 days. As a noble gas, radon emanates from the Earth’s surface into the atmosphere where it decays via the very short-lived intermediate nuclides 218Po, 214Pb, 214Bi and 214Po (all having half-lives shorter than 30min) into 210Pb. 210Pb has a half-life of 22.3 years and decays into its daughter 210Bi with a half-life of 5 days, which itself decays into a ‘granddaughter’ 210Po with a half-life of 138.4 days. This means that after several half-lives of 210Po, i.e. ~1 year, the activity concentrations of all three nuclides, i.e. of 210Pb, 210Bi and 210Po, are equal (secular equilibrium). With the emission of an alpha particle, 210Po finally decays into the stable 206Pb, the end product of the 238U decay series (Reference Benoit and HemondBenoit and Hemond, 1987). Hence, the activity concentration of 210Pb can be measured by analyzing either 210Pb itself or 210Bi or 210Po after several half-lives of these progenies. Since detection of a-particles from the decay of 210Po is very sensitive and nuclide-specific, in contrast to β-particles emitted by 210Pb or 210Bi, it is advisable to determine the activity concentration of 210Pb in ice cores by analyzing the 210Po activity.

The first attempts to date ice layers using the 210Pb method were made by Reference GoldbergGoldberg (1963). Later, Reference Krishnaswamy and LalKrishnaswamy and Lal (1971) and Reference Koide, Soutar and GoldbergKoide and others (1972) made an exploratory study of 210Pb dating on lake waves and the gulf sediments. Gaggeler and others (1983) proved for the first time that the 210Pb dating method was a useful tool for dating cold high-altitude alpine glaciers. This approach has since been used to date a number of ice cores (e.g. from Illimani, Bolivia (Reference KnüselKnüsel and others, 2003); Cerro Tapado (Reference Ginot, Kull, Schotterer, Schwikowski and GäggelerGinot and others, 2006) and Monte San Valentin, Chile (Reference VimeuxVimeux and others, 2008)). However, until now there has been no reported 210Pb dating of ice cores from the Tibetan Plateau and surrounding regions. In this study, we used 210Pb to date the Miaoergou ice core drilled from the eastern Tien Shan, China.

β-activity measurements and annual-layer counting are two of the main approaches used in mountain ice-core dating. β-activity dating is based on the identification of late 1950s and early 1960s radioactive debris from nuclear weapons testing around the world, with a peak activity in the Northern Hemisphere around AD 1962-63. Annual-layer counting can be used to determine ice-core age by studying physical and chemical indicators of species that exhibit seasonal changes in the ice-core record. Examples are δ18O or chemical species that exhibit seasonal variability (e.g. ammonia from agricultural activity). As ice cores are subjected to annual-layer thinning with increasing depth, the method can only determine the age of the upper part of the ice core, i.e. is limited to a relatively short period. The 210Pb dating method yields a continuous age-depth relationship for up to two centuries and has been widely used in recent years (Knusel and others, 2003; Reference Cecil, Green and ThompsonCecil and others, 2004; Reference Ginot, Kull, Schotterer, Schwikowski and GäggelerGinot and others, 2006; Reference VimeuxVimeux and others, 2008).

Some assumptions have to be made for successful application of the 210Pb dating method. The amount of supported 210Pb coming from the 238U content in mineral dust contained in the ice should be constant and the mean 210Pb activity in precipitation should have remained constant during the dating period (CF:CS model assumption, where CF stands for constant rate of supply and CS for constant activity concentration in precipitation (Reference ApplebyAppleby, 2001). Moreover, there should be no significant transport of 210Pb by percolating meltwater. During the warm season, in daytime the air temperature may rise above 0°C. However, the formed meltwater will refreeze during the night (Reference ShumskiyShumskiy, 1964) or due to the negative temperatures inside the ice (Reference Liu, Hou, Ren and Wang Yand GenLiu and others, 2006). The night temperature decreased from –2.92°C at 1m to –7.62°C at 8m depth and gradually increased to –6.25°C from 8 to 20 m depth (Reference Song, Hou and LiuSong and others, 2011). We therefore conclude that the melting process has little impact on the 210Pb dating.

Materials and Methods

Ice-core sampling

The Miaoergou flat-topped glacier covers an area of -3.45 km2. Its altitude from the summit to the ice tongue ranges from 4512 to 3840 m, and the equilibrium-line altitude is ~4100ma.s.l. (LIGG, 1986). In 2005, two ice cores to bedrock (58.7 and 57.6 m length for cores 1 and 2, respectively) were recovered from a dome on Miaoergou glacier (43° 03 ʹ19ʺN, 94°19ʹ21ʺE; 4512ma.s.l.) (Reference Liu, Hou, Hong, Soon, Lee and WangLiu and others, 2011; Fig. 1). The low borehole temperature at the drilling site (-7.2°C at 10 m depth and -8.2°C at the bottom) is beneficial for the preservation of ice-core records (Reference Liu, Hou, Wang and SongLiu and others, 2009). The ice cores were transported frozen to the State Key Laboratory of Cryospheric Sciences, Lanzhou, China, for processing. A first study of trace elements contained in core 2 was performed down to 17 m (14 m w.e.) (Reference Liu, Hou, Hong, Soon, Lee and WangLiu and others, 2011). Besides some heavy metals, the bomb peak assigned to the period AD 1962-63 was also found at ~12.5 m depth (11 m w.e.) by total β-counting of 90Sr and 90Y in the ice samples (Reference Liu, Hou, Hong, Soon, Lee and WangLiu and others, 2011). This yielded an average net annual accumulation rate of 259 mm w.e. a-1. From annual-layer counting based on heavy-metal concentrations, an age of AD 1953 was deduced at 17m depth (14 m w.e.), resulting in an average net accumulation rate of 269 mm w.e. a–1. The analysis was stopped at 17m depth (assigned to AD 1953) due to lack of dating of the deeper part of the core. In this paper, we present a further dating of core 2 using the 210Pb dating method.

Fig. 1. Location of the Miaoergou flat-topped glacier in the eastern Tien Shan, China. The black dot shows the position of the drilling site (4380301900 N, 9481902100 E; 4512ma.s.l.).

Experiment

The ice samples are processed according to the standard method established by Gaggeler and others (2011). Each of the ice samples was cut parallel to the drilling axis in a -18°C cold room at the State Key Laboratory of Cryospheric Sciences. The weight of each sample was -300 g. Each sample was melted after adding 10mL conc. HCl, 1g NH4OH-HCl per 100g ice. NH4OH-HCl served as a reducing agent to ensure polonium stays in an elemental state in the acidified solution. Then 100 mL 209Po tracer was added to the solution to determine the yield of the separation. Spontaneous deposition of Po on an Ag disk (15 mm diameter), which was fixed on a wire and immersed in the liquid, was achieved during - 8 hours at 95°C in 500 mL Erlenmeyer flasks using a magnetic stirrer. Typical chemical and counting yields were -80%. After drying, the disks were transferred to the University of Bern for accounting. The samples were positioned in vacuum chambers at a distance of 1 mm from silicon surface barrier detectors (ORTEC, ruggedized, 300 and 450 mm2) having an a-energy resolution of - 2 3 keV full width at half-maximum (FWHM) at 5.3 MeV. The yield of 209Po tracer was measured via its 4.9 MeV a-line. Typical counting yields were -45%.

Age calculation method

The 210Pb activity concentration of glacier ice has two components: a supported component derived from the 238U (equal to the 226Ra) decay rate, and an unsupported (or excess) component derived from the atmospheric fallout of 210Pb (marked as 210Pbex). Supported 210Pb is deposited by aerosol particles that contain 238U, while excess 210Pb is deposited through decay from atmospheric 222Rn and later attachment of formed 210Pb to the surface of particulate matter (Fig. 2). The supported 210Pb activity can be determined by measuring the value of the experimental background at ages not accessible by the 210Pb method (Reference WanWan, 1997), and the excess 210Pb activity can be determined by subtracting the supported 210Pb activity from the total 210Pb activity concentration (marked as 210Pbtot) (Reference Appleby and OldfieldAppleby and Oldfield, 1983). The age of an ice core can then be calculated applying the decay law to the measured 210Pbex activities along the ice core. As the supported 210Pb values are assumed to be constant along the ice core, the age was calculated using the 210Pbex values applying the CF:CS model. This model assumes a constant rate of deposition, i.e. of annual precipitation rates, and that the activity concentration of 210Pb in precipitation remained constant over time, independent of the amount of precipitation during a given snowfall (Reference WanWan, 1997; Xia and Xue, 2004; Reference Zhang and LiuZhang and others, 2008, 2012).

Fig. 2. Sketch of a glacier profile showing the main sources of 210Pb. The 210Pb activity of glacier sediments has two components: a supported component deriving from the 2 3 8U (equal to the 226Ra) decay, and an unsupported (or excess) component deriving from the atmospheric fallout of 210Pb (marked as 210Pbex).

Results and Discussion

The 210Pb activity profile

The record of the 210Pbtot activity concentrations measured along the ice core is depicted in Figure 3, which shows an exponential decrease as a function of depth in line with the radioactive decay law. The 210Pbtot activity concentrations below 35.2 mw.e. down to bedrock were constant, with a value of 5.48±0.16 mBq kg–1. This value was taken as supported 210Pb from the mineral dust contained in the ice core and was therefore subtracted from all total 210Pb activity concentration above 35.2 mw.e. to obtain the 210Pbex values.

Fig. 3. Correlation between 210Pbt o t activity concentrations and depth of ice core from Miaoergou flat-topped glacier. An exponential fit function was applied to the scatter plots, and the coefficient of determination (r 2) was 0.987. The 210Pbto t activity concentrations show a negative exponential decrease as function of depth in line with radioactive decay law.

The data depicted in Figure 4 represent the resulting 210Pbex activity concentrations as a function of depth. We observed some fluctuations in the exponential decrease of the 210Pbex activity concentrations, which we ascribe to variations in precipitation rates (see below). This indicates that the input of 210Pb at this drilling site was on average constant during the dating period, in accord with the assumption of the CF:CS dating model. From the linear regression of the logarithmic 210Pb activities against depth we conclude that at a depth of 35.2 mw.e. of ice core the year AD 1851 ± 6 is reached. The value of the axis intercept (~400 mBq kg–1) corresponds to the 210Pbex activity at the surface of Miaoergou glacier. From the slope of the regression line, we derive a mean annual net accumulation rate of 229±7mmw.e.a-1. The estimated age-depth relation has an uncertainty of ±6 years.

Fig. 4. 210Pbex activity concentrations (scatter plots, left-hand logarithmic scale), annual-layer counting (solid line) and β-counting (bars) of ice core from Miaoergou flat-topped glacier. The rightmost axis depicts the age deduced from the 210Pbex measurement. The estimated age-depth relation has uncertainties of ±6 years. The dot-dashed line indicates the average 210Pb decrease. The dashed line indicates the bomb horizon deduced from β-counting assigned to the period AD 1962-63, which agrees well with the results of annual-layer counting and the 210Pb dating method.

Figure 4 compares the 210Pb dating results with the chronological sequence obtained from annual-layer counting results (until 1953) and the β-counting method which assays the β-activity peak of 90Sr and 90Y from the atmospheric nuclear testing period AD 1962-63. The 210Pb dating agrees within error well with the bomb horizon during AD 1962-63 at 11 mw.e. but also with the annual counting result of AD 1953 at 14mw.e. The results of different dating methods are therefore highly consistent, indicating that the result of the 210Pb dating method applied to the Miaoergou ice core is reliable. The linear decay of the depicted 210Pbex activity concentrations with depth also corroborates the assumption that no significant thinning of the ice core can be observed down to 35.2 mw.e.

210Pbex activity at the surface

The surface activity concentration of ~400 mBq kg–1 is remarkably high, even higher than observed at other continental sites such as at Belukha, Russia (280 mBq kg–1; Reference OlivierOlivier and others, 2006), or nearby Tsambagarav, Mongolia (Reference Herren, Türler, Schwikowski and BlattmannHerren and others, 2011), with the same surface activity concentration. This means that the 222Rn concentration in air in the eastern Tien Shan must be very high and the 238U concentration in soil of the regional environment must also be high. In addition, emanation of 222Rn is closely related to the geographical and climatic conditions of the study area. Any changes in atmospheric pressure, temperature, weather conditions, soil moisture, vegetation coverage, etc., will affect the release of 222Rn from the Earth’s surface, and thus affect the 210Pb concentration in the atmosphere. It might therefore be desirable to measure 222Rn activity concentrations in the study area as well as 238U concentration values in soil.

Mean net accumulation rates

Glaciers in this area near the Gobi Desert are the major water supply for the extremely arid land of Hami, an oasis city close to the Miaoergou flat-topped glacier. Reference Luo, Qi, Xu and LiLuo and others (2002) and Reference Zhang and LiuZhang and Liu (2011) pointed out that, based on field studies, precipitation rates in the area above 4000 ma.s.l. in the Yushugou basin (438020-438110 N, 938570-948190E) are up to 400-500 mm a–1. This value is in reasonably good agreeement with our value of 229±7 mmw.e.a-1. From the 1957-2005 precipitation data at Hami weather station we obtain an average annual precipitation rate of 38 mm a–1 (Fig 5). The precipitation rates at Hami show a weak trend towards increasing values, in accordance with the trend of warmer and wetter climate in northwest China (Reference ShiShi and others, 2003).

Fig. 5. Changes in net accumulations of Miaoergou flat-topped glacier from AD 1851 to 2005 deduced from the 2 1 0Pbe x values and the precipitations of Hami from AD 1957 to 2005. For the period 1851–2005, we calculated the net accumulations at different time intervals according to the results of the 2 1 0Pb dating method. For the period 1957–2005, we calculated the precipitations of Hami at the same time intervals as the net accumulations.

Conclusions

The 210Pb dating method has been applied to a 57.6 m ice core from Miaoergou glacier recovered at 4512ma.s.l. in 2005. The investigated samples have been worked up for 210Po which was assayed by a-spectroscopy to deduce the 210Pb activity concentration at secular equilibrium. The surface activity concentration of 210Pbex at this site is ~400 mBq kg–1 which is very high compared to other sites worldwide. Using the 210Pb CF:CS dating model, we conclude that at a depth of 35.2 mw.e. the year AD1851 ±6 is reached The resulting mean net annual accumulation rate is 229±7mmw.e.a-1. The results of the 210Pb dating method, of annual-layer counting and of β-counting are highly consistent, which indicates that the result of the 210Pb dating method applied to the Miaoergou ice core is reliable and can be used to date the ice core to ages older than 1953, the limiting age prior to this study.

This work shows for the first time that 210Pb dating is a suitable method for dating glaciers in the eastern Tien Shan. This method could also be used to date other ice cores recovered from the mountains of western China.

Acknowledgements

We greatly appreciate the efforts of all field personnel on the scientific expedition to the Miaoergou flat-topped glacier in 2005. This research was funded by the National Natural Science Foundation of China (41330526, 41171052, 41321062 and 40825017), the National Basic Research Program of China (2010CB951401), the Chinese Academy of Sciences (XDB03030101-4) and the Fundamental Research Funds for the Central Universities (1082020904, 20110091110025). H.W.G. greatly appreciates the hospitality he received during his visit to Nanjing University.

References

Alley, RB and 11 others (1997) Visual-stratigraphic dating of the GISP2 ice core: basis, reproducibility, and application. J. Geophys. Res., 102(C12), 26 367–26 382 (doi: 10.1029/ 96JC03837)Google Scholar
Appleby, PG (2001) Chronostratigraphic techniques in recent sediments. In Last WM and Smol JP eds. Tracking environmental change using lake sediments. Vol. 1: Basin analysis, coring, and chronological techniques. Kluwer, Dordrecht, 171–203 Google Scholar
Appleby, PG and Oldfield, F (1983) The assessment of 210Pb data from sites with varying sediment accumulation rates. Hydrobiologia, 103(1), 29–35 (doi: 10.1007/BF00028424)CrossRefGoogle Scholar
Barbante, C and 14 others (2004) Historical record of European emissions of heavy metals to the atmosphere since the 1650s from alpine snow/ice cores drilled near Monte Rosa. Environ. Sci. Technol., 38(15), 4085–4090 (doi: 10.1021/es049759r)CrossRefGoogle Scholar
Benoit, G and Hemond, HF (1987) A biogeochemical mass balance of 210Po and 210Pb in an oligotrophic lake with seasonally anoxic hypolimnion. Geochim. Cosmochim. Acta, 51(6), 1445–1456 (doi: 10.1016/0016-7037(87)90327-9)CrossRefGoogle Scholar
Cecil, LD, Green, JR and Thompson, LG (2004) Earth paleoenvironments: records preserved in mid- and low-latitude glaciers. Kluwer Academic, Dordrecht Google Scholar
Ciais, P, Jouzel, J, Petit, JR, Lipenkov, V and White, JWC (1994) Holocene temperature variations inferred from six Antarctic ice cores. Ann. Glaciol., 20, 427–436 CrossRefGoogle Scholar
Cole-Dai, J, Mosley-Thompson, E, Wight, SP and Thompson, LG (2000) A 4100-year record of explosive volcanism from an East Antarctic ice core. J. Geophys. Res., 105(D19), 24431–24441 (doi: 10.1029/2000JD900254)Google Scholar
Dansgaard, W and 10 others (1993) Evidence for general instability of past climate from a 250-kyr ice-core record. Nature, 364(6434), 218–220 (doi: 10.1038/364218a0)CrossRefGoogle Scholar
Eichler, A and 7 others (2000) Glaciochemical dating of an ice core from upper Grenzgletscher (4200 m a.s.l.). J. Glaciol., 46(154), 507–515 (doi: 10.3189/172756500781833098)Google Scholar
EPICA Community Members (2004) Eight glacial cycles from an Antarctic ice core. Nature, 429(6992), 623–628 (doi: 10.1038/ nature02599)Google Scholar
Gäggeler, H, Von Gunten, HR, Rössler, E, Oeschger, H and Schotterer, U (1983) 210Pb-dating of cold Alpine firn/ice cores from Colle Gnifetti, Switzerland. J. Glaciol., 29(101), 165–177 CrossRefGoogle Scholar
Gäggeler, HW and 15 others (2011) 210Pb dating of the Mt Hutton ice core from New Zealand. In Türler, A, Schwikowski, M and Blattmann, A eds. Annual Report: Labor für Radio-und Umweltschemie 2010. Paul Scherrer Institut, Universität Bern, Bern, 64Google Scholar
Ginot, P, Kull, C, Schotterer, U, Schwikowski, M and Gäggeler, HW (2006) Glacier mass balance reconstruction by sublimation induced enrichment of chemical species on Cerro Tapado (Chilean Andes). Climate Past, 2(1), 21–30 (doi: 10.5194/cp-2-21-2006)Google Scholar
Goldberg, ED (1963) Geochronology with lead-210. In.Radioactive dating: Proceedings of a Symposium on Radioactive Dating, 19–23 November 1962, Athens, Greece. International Atomic Energy Agency, Vienna, 121–131 Google Scholar
Herren, P-A and 6 others (2011) Dating an ice core from the Tsambagarav, Mongolian Altai. In Türler, A, Schwikowski, M and Blattmann, A eds. Annual Report: Labor für Radio- und Umweltschemie 2010. Paul Scherrer Institut, Universität Bern, Bern, 21 Google Scholar
Hou, S, Qin, D, Zhang, D, Kang, S, Mayewski, PA and Wake, CP (2003) A 154 a high-resolution ammonium record from the Rongbuk Glacier, north slope of Mt. Qomolangma (Everest), Tibet–Himal region. Atmos. Environ., 37(5), 721–729 (doi: 10.1016/S1352- 2310(02)00582-4)Google Scholar
Johnsen, SJ, Dansgaard, W, Clausen, HB and Langway, CC, Jr (1972) Oxygen isotope profiles through the Antarctic and Greenland ice sheets. Nature, 235(5339), 429–434 (doi: 10.1038/235429a0)CrossRefGoogle Scholar
Kang, S, Mayewski, PA, Yan, Y and Qin, D (2003) Dust records from three ice cores: relationships to spring atmospheric circulation over the Northern Hemisphere. Atmos. Environ., 37(34), 4823–4835 (doi: 10.1016/j.atmosenv.2003.08.010)Google Scholar
Knüsel, S and 8 others (2003) Dating of two nearby ice cores from the Illimani, Bolivia. J. Geophys. Res., 108(D6), 4181 (doi: 10.1029/2001JD002028)Google Scholar
Koide, M, Soutar, A and Goldberg, ED (1972) Marine geochronology with 210Pb. Earth Planet. Sci. Lett., 14(3), 442–446 (doi: 10.1016/0012-821X(72)90146-X)CrossRefGoogle Scholar
Krishnaswamy, S and Lal, D (1971) Geochronology of lake sediments. Earth Planet. Sci. Lett., 11(1–5), 407–414 (doi: 10.1016/0012-821X(71)90202-0)Google Scholar
Lanzhou Institute of Glaciology and Geocryology (LIGG) (1986) Glacier Inventory of China III. Tien Shan mountains (Ili River drainage basin), ed. Ding, L, Xie, W, Liu, C, Wang, C and Wang, Z. Science Press, Academia Sinica, Beijing [in Chinese]Google Scholar
Legrand, MR and Delmas, RJ (1987) A 220-year continuous record of volcanic H2SO4 in the Antarctic ice sheet. Nature, 327(6124), 671–676 (doi: 10.1038/327671a0)Google Scholar
Liu, Y, Hou, S, Ren, J, Wang Yand Gen, Z (2006) Distribution features of borehole temperatures in the Miaoergou flat-topped glacier, East Tianshan Mountains. J. Glaciol. Geocryol., 28(5), 668–671 [in Chinese with English summary]Google Scholar
Liu, Y, Hou, S, Wang, Y and Song, L (2009) Distribution of borehole temperature at four high-altitude alpine glaciers in Central Asia. J. Mt. Sci. [China], 6(3), 221–227 (doi: 10.1007/s11629-009-0254-9)Google Scholar
Liu, Y, Hou, S, Hong, S, Soon, DH, Lee, K and Wang, Y (2011) High-resolution trace element records of an ice core from the eastern Tien Shan, central Asia, since 1953 AD. J. Geophys. Res., 116(D12), D12307 (doi: 10.1029/2010JD015191)Google Scholar
Luo, GX, Qi, XM, Xu, LC and Li, B (2002) Hydrological characteristics of the Yushugou valley. Xinjiang Meteorol. Bi-monthly, 25(5), 17–20 [in Chinese]Google Scholar
Meese, DA and 8 others (1997) The Greenland Ice Sheet Project 2 depth–age scale: methods and results. J. Geophys. Res., 102(C12), 26411–26423 (doi: 10.1029/97JC00269)Google Scholar
North Greenland Ice Core Project (NorthGRIP) Members (2004) High-resolution record of Northern Hemisphere climate extending into the last interglacial period. Nature, 431(7005), 147–151 (doi: 10.1038/nature02805)CrossRefGoogle Scholar
Oeschger, H and JrLangway, CC (1989) The environmental record in glaciers and ice sheets. (Wiley Physical, Chemical, and Earth Sciences Research Report 8) Wiley, Chichester Google Scholar
Olivier, S and 10 others (2003) Glaciochemical investigation of an ice core from Belukha glacier, Siberian Altai. Geophys. Res. Lett., 30(19), 2019 (doi: 10.1029/2003GL018290)Google Scholar
Olivier, S and 8 others (2006) Temporal variations of mineral dust, biogenic tracers, and anthropogenic species during the past two centuries from Belukha ice core, Siberian Altai. J. Geophys. Res., 111(D5), D05309 (doi: 10.1029/2005JD005830)Google Scholar
Petit, JR and 18 others (1999) Climate and atmospheric history of the past 420,000 years from the Vostok ice core, Antarctica. Nature, 399(6735), 429–436 (doi: 10.1038/20859)CrossRefGoogle Scholar
Pourchet, M, Pinglot, JF and Lorius, C (1983) Some meteorological applications of radioactive fallout measurements in Antarctic snows. J. Geophys. Res., 88(C10), 6013–6020 (doi: 10.1029/ JC088iC10p06013)Google Scholar
Raisbeck, GM and Yiou, F (1985) 10Be in polar ice and atmospheres. Ann. Glaciol., 7, 138–140 CrossRefGoogle Scholar
Raisbeck, GM, Yiou, F, Bourles, D, Lorius, C, Jouzel, J and Barkov, NI (1987) Evidence for two intervals of enhanced 10Be deposition in Antarctic ice during the last glacial period. Nature, 326(6110), 273–277 (doi: 10.1038/326273a0)Google Scholar
Shen, L and 7 others (2012) Variation of culturable bacteria along depth in the East Rongbuk ice core, Mt. Everest. Geosci. Frontiers, 3(3), 327–334 (doi: 10.1016/j.gsf.2011.12.013)Google Scholar
Shi, Y and 6 others (2003) Discussion on the present climate change from warm-dry to warm-wet in northwest China. Quat. Sci., 23(2), 152–164 [in Chinese with English summary]Google Scholar
Shumskiy, PA (1964) Principles of structural glaciology. Dover Publications, New York Google Scholar
Song, L, Hou, S and Liu, Y (2011) d18O record of the Miaoergou ice core from the Karlik mountains of east Tienshan since 1953. J. Lanzhou Univ. (Natur. Sci.), 47(5), 36–41 [in Chinese]Google Scholar
Svensson, A and 7 others (2005) Visual stratigraphy of the North Greenland Ice Core Project (NorthGRIP) ice core during the last glacial period. J. Geophys. Res., 110(D2), D02108 (doi: 10.1029/2004JD005134)Google Scholar
Vimeux, F and 7 others (2008) A promising location in Patagonia for paleoclimate and paleoenvironmental reconstructions revealed by a shallow firn core from Monte San Valentın (Northern Patagonia Icefield, Chile). J. Geophys. Res., 113(D16), D16118 (doi: 10.1029/2007JD009502)Google Scholar
Wan, GJ (1997) 210Pb dating for recent sedimentation. Quat. Sci., 3, 231–239 [in Chinese]Google Scholar
Wang, X, Gong, P, Zhang, Q and Yao, T (2010) Impact of climate fluctuations on deposition of DDT and hexachlorocyclohexane in mountain glaciers: evidence from ice core records. Environ. Poll., 158(2), 375–380 (doi: 10.1016/j.envpol.2009.09.006)Google Scholar
Wu, G and 6 others (2013) Atmospheric dust from a shallow ice core from Tanggula: implications for drought in the central Tibetan Plateau over the past 155 years. Quat. Sci. Rev., 59, 57–66 (doi: 10.1016/j.quascirev.2012.10.003)Google Scholar
Xu, J and 10 others (2010) A 108.83-m ice-core record of atmospheric dust deposition at Mt. Qomolangma (Everest), Central Himalaya. Quat. Res., 73(1), 33–38 (doi: 10.1016/j.yqres.2009.09.005)Google Scholar
Yang, M, Yao Tand Wang, H (2006) Microparticle content records of the Dunde ice core and dust storms in northwestern China. J. Asian Earth Sci., 27(2), 223–229 (doi: 10.1016/j.jseaes.2005. 03.007)CrossRefGoogle Scholar
Zhang, HY and Liu, H (2011) Analysis of hydrology and water resources in Yushugou valley, Xinjiang. Heilongjiang Sci. Technol. Water Conserv., 39(5), 8–9 [in Chinese]Google Scholar
Figure 0

Fig. 1. Location of the Miaoergou flat-topped glacier in the eastern Tien Shan, China. The black dot shows the position of the drilling site (4380301900 N, 9481902100 E; 4512ma.s.l.).

Figure 1

Fig. 2. Sketch of a glacier profile showing the main sources of 210Pb. The 210Pb activity of glacier sediments has two components: a supported component deriving from the 2 3 8U (equal to the 226Ra) decay, and an unsupported (or excess) component deriving from the atmospheric fallout of 210Pb (marked as 210Pbex).

Figure 2

Fig. 3. Correlation between 210Pbt o t activity concentrations and depth of ice core from Miaoergou flat-topped glacier. An exponential fit function was applied to the scatter plots, and the coefficient of determination (r2) was 0.987. The 210Pbto t activity concentrations show a negative exponential decrease as function of depth in line with radioactive decay law.

Figure 3

Fig. 4. 210Pbex activity concentrations (scatter plots, left-hand logarithmic scale), annual-layer counting (solid line) and β-counting (bars) of ice core from Miaoergou flat-topped glacier. The rightmost axis depicts the age deduced from the 210Pbex measurement. The estimated age-depth relation has uncertainties of ±6 years. The dot-dashed line indicates the average 210Pb decrease. The dashed line indicates the bomb horizon deduced from β-counting assigned to the period AD 1962-63, which agrees well with the results of annual-layer counting and the 210Pb dating method.

Figure 4

Fig. 5. Changes in net accumulations of Miaoergou flat-topped glacier from AD 1851 to 2005 deduced from the 2 1 0Pbe x values and the precipitations of Hami from AD 1957 to 2005. For the period 1851–2005, we calculated the net accumulations at different time intervals according to the results of the 2 1 0Pb dating method. For the period 1957–2005, we calculated the precipitations of Hami at the same time intervals as the net accumulations.