Introduction

Ice-core chemistry records contain climatic and environmental information over a wide range of timescales. The records preserved in glaciers, however, are determined not only by the atmospheric concentration of the physical and chemical species and the processes involved in their deposition, but also by post-depositional processes such as melting, percolation, sublimation, wind filtration through firn (which involves mass loss, addition and/or exchange) and diffusion (Reference Dibb, Wolff and BalesDibb, 1996; Reference Waddington, Cunningham, Harder, Wolff and BalesWaddington and others, 1996; Reference Wolff, Wolff and BalesWolff, 1996; Reference Ginot, Kull, Schwikowski, Schotterer, Pouyaud and GäggelerGinot and others, 2001; Reference Stichler, Schotterer, Fröhlich, Ginot, Kull and GäggelerStichler and others, 2001; Reference Schotterer, Stichler, Ginot, Cecil, Green and ThompsonSchotterer and others, 2004; Reference Schulz and de JongSchulz and de Jong, 2004).

In order to better understand the deposition and post-depositional processes controlling the chemical signals recorded in glacial snow and ice, the Program for Glacier Processes Investigation (PGPI) has examined the seasonal variation and evolution of Mg²⁺, Ca²⁺ and microparticle concentrations in 54 profiles collected over 12 months from a snow pit on Ürümqi glacier No. 1 (UG1), located in the eastern Tien Shan, northwestern China. Several similar studies have been accomplished on other alpine glaciers, (e.g. Reference Psenner and NickusPsenner and Nickus, 1986; Reference Neftel, Sigg, Zürcher, Angletti and RestelliNeftel and others, 1987; Reference PuxbaumPuxbaum 1989; Reference Maupetit, Borrell, Borrell, Cvitas and SeilerMaupetit and others, 1993; Reference Kuhn, Haslhofer, Nickus and SchellanderKuhn and others, 1998; Reference WiniwarterWiniwarter and others, 1998; Reference Iizuka, Igarashi, Kamiyama, Motoyama and WatanabeIizuka and others, 2002; Reference PohjolaPohjola and others, 2002; Reference Schotterer, Stichler, Ginot, Cecil, Green and ThompsonSchotterer and others, 2004), but only a few studies (Hou and Qin, 1996, Reference Hou and Qin1999; Reference Hou, Qin and RenHou and others, 1999) have been conducted in this region of the Tien Shan.

The Setting and Glaciology of the Sampling Site

UG1 is located at the Ürümqi riverhead adjacent to the vast deserts and dried lakes of central Asia and far from densely populated areas. The glacier itself is composed of east and west branches which flow around a mass of exposed bedrock and moraine sediment, the chemical composition of which is rich in such species as sodium, calcium, magnesium and iron (Reference LuoLuo, 1983). The prevailing westerlies flow over the mountain range, but the topography distorts the wind flow into cyclonic and anticyclonic circulation patterns up to 4000 m a.s.l. Near the surface, the local valley winds prevail from March through September (Reference Zhang, Kang and LiuZhang and others, 1994). Typically, 90% of the precipitation in this region occurs between May and September.

From 1959 to 2003, the annual equilibrium-line altitude (ELA) of the glacier has averaged approximately 4055 m a.s.l. An observation and experimental site was carefully chosen in a percolation zone of the east branch of UG1 (where the ice surface slopes about 6˚) above the ELA at 4130 m a.s.l. Here the overshadowing of the mountain ridges prevents direct exposure to sunshine in the winter. During the sampling period, the mean annual air temperature was about −9.1 ˚C, and the precipitation, i.e. snowfall, was approximately 700 mm w.e.

The stratigraphic sequence of the pit from top to bottom can be described as fresh snow, coarse-grained snow, finegrained firn, firn and coarse-grained firn. The fresh snow and coarse-grained snow were derived from the accumulation of the most recent year, while the underlying firn layers were from previous years. The floor of the pit was made of ‘infiltration-congelation ice’ (Reference ShumskiiShumskii, 1964), or superimposed ice (Reference PatersonPaterson, 1994), which was characterized by clear and impermeable opaque ice with spherical bubbles - 1 - 5 mm in diameter. The depth typically ranged from about 1.5 m when the study began in the late summer to about 3 m in the late spring, but during the winter it remained stable because of snow compaction, drifting and sublimation. In the early summer, as air temperature rose to ∼0˚C, the upper part of the snow layer began to melt, which led to a rapid thinning. The melting primarily involved the accumulation from the previous autumn. During the late summer to the early autumn, the melting impacted the entire annual layer, and even included the underlying accumulation from the previous year. The meltwater infiltrated to the underlying firn layers, reaching the impermeable superimposed ice formed the previous year. The water filled the pores and was refrozen to form new superimposed ice, while some of the meltwater pooled on the ice surface and eventually drained off.

Methodology

At the PGPI site, both surface snow and snow-pit samples were collected from September 2003 to September 2004 on a weekly basis. We tried to collect the fresh snow and well-preserved surface snow (i.e. snow that was not affected by post-depositional processes such as sublimation or melting) at the sampling site each week to investigate the chemical seasonality in precipitation and dry deposition. Therefore, during the winter season when there was insufficient snowfall, we usually sampled the topmost 3cm. However, if an accumulation event occurred prior to the sampling, we collected the top 1 cm of the fresh snow. During the summer, there was usually sufficient fresh snow available, and samples from accumulation that was no more than 2days old were usually collected from the top 3–5 cm. Over the year a total of 54 surface snow samples were retrieved, but 9 samples were discarded for analysis because of problems associated with in situ melting.

The pit was also sampled from top to bottom at 10 cm increments 54 times during the year on a weekly basis to yield a total of 1011 samples. After each session, the pit was refilled and 7 days later was re-excavated. The wall was then scaled back by at least 50 cm before the next round of collecting. A strict protocol was followed during this procedure to prevent contamination, including the use of disposable polyethylene gloves, masks and pre-cleaned polyethylene sample containers. All the samples were transported in insulated boxes to the Tien Shan Glaciological Station (TGS) laboratory, and were kept frozen until analysis.

Insoluble particles, Ca²⁺ and Mg²⁺ were analyzed in the TGS laboratory. All sample handling was done in a class 100 clean room in order to minimize contamination. The Ca²⁺ and Mg²⁺ concentrations were measured by ion chromatography using a Dionex DX-320 system with a CS12A separation column. The detection limits of Mg²⁺ and Ca²⁺ are 0.8 and 0.75 ngg⁻¹, respectively (Reference Zhao and LiZhao and Li, 2004). Microparticle concentrations and size distributions were measured with an AccuSizer 780A which uses Single Particle Optical Sensing (SPOS) technology and measures in 8–512 size channels, with an error of <5% in the 0.5– 400 μm measuring range. Prior to analysis, samples were melted at room temperature while the pipeline and AccuSizer system were cleaned with Milli-Q water until the background particle count was <50mL⁻¹.

Results and Discussion

Processes involved in the post-depositional modification of the aerosol stratigraphy

Although the processes involved in the post-depositional modification of the insoluble and soluble aerosols were different, the stratigraphy of the pits indicates that the dust layers occurred coincidentally with increases in Ca²⁺ and Mg²⁺, which suggests that these species were not leached out from the dust. The linear correlation coefficient (r) of each ion with the large particles (>10 μm in diameter) is significant; for Mg²⁺, r = 0.74 and for Ca²⁺, r = 0.85 (two-tailed, p = 0.01, N = 107). Slight seasonal differences in the microparticle, Mg²⁺ and Ca²⁺ concentrations in the surface snow may be due to the aerosols being derived from separate sources. However, after being deposited into the snow, they experienced post-depositional alteration mainly controlled by meltwater percolation. It was determined that the development of the aerosol stratigraphies was closely related to the physical development of the snow–firn pack such that both experienced a similar evolution process (Fig. 1).

Fig. 1.

The relationship between the snow stratigraphy and the Mg²⁺, Ca²⁺ and large particle concentration profiles in the snow pit on selected sampling days (dates are mm/dd/yy). These profiles were selected from among the 54 that were created from the weekly sampling in order to illustrate seasonal changes. The y axis presents height (cm w.e.) above the surface of the superimposed ice.

Figure 2 illustrates the evolution processes of the Mg²⁺ in the snow pits from September 2003 to September 2004 (the evolution processes of Ca²⁺ and microparticles in the snow pit are identical to Mg²⁺). In mid-September 2003, there were three marked Mg²⁺ peaks (P1, P2 and P3) in the firn at heights of 89, 62 and 34 cm, respectively, above the superimposed ice. From mid-September to mid-November 2003, P1, P2 and P3 moved downward to heights of 80, 55 and 16 cm, respectively, from the bottom of the pit, and this movement was mainly related to snow compaction. During the period mid-November 2003 to late April 2004, several small concentration peaks appeared in the upper part of the snow pits. These resulted from limited precipitation, low temperatures and weak evaporation (Reference Ginot, Kull, Schwikowski, Schotterer, Pouyaud and GäggelerGinot and others, 2001; Reference Stichler, Schotterer, Fröhlich, Ginot, Kull and GäggelerStichler and others, 2001; Reference Schulz and de JongSchulz and de Jong, 2004) at the site, which enabled post-depositional processes such as sublimation and dry deposition to become more dominant. As the temperature increased from April to late May, meltwater appeared in the pit, which attenuated the peaks as they moved downward. At the same time, the increasing precipitation resulted in successive concentration peaks at about 10–30 cm below the surface. In the summer (June–August), as meltwater percolated through the pit, it leached the ions, including Ca²⁺ and Mg²⁺ (Reference Brimblecombe, Tranter, Abrahams, Blackwood, Davies and VincentBrimblecombe and others, 1985, Reference Brimblecombe, Clegg, Davies, Shooter and Tranter1987; Reference Tranter, Tsiouris, Davies and JonesTranter and others, 1992; Reference Eichler, Schwikowski and GäggelerEichler and others, 2001). During this period, the upper part of the snow pit experienced the most post-depositional alteration. With increasing temperature, larger volumes of meltwater began to percolate deeper into the pit along with the Mg²⁺, which is indicated by the displacement and reduced concentration of the peaks. When the water encountered the superimposed ice in the bottom of the coarse-grained firn layer, it refroze, resulting in accretion (mass gain) at the superimposed ice surface. This strong ablation caused the melding of the P3 layer with the surface layers. At the end of August, P1 merged into the superimposed ice at the bottom of the pit and was henceforth preserved in the glacier. By the beginning of September 2004, there were only two peaks observed in the snow pit. This demonstrates that in spite of considerable loss of Mg²⁺ through post-depositional processes, the general information is still preserved.

Fig. 2.

The evolution process of vertical profiles of Mg²⁺ in snow pits from 13 September 2003 to 8 September 2004 (dates are mm/ dd/yy). P 1 , P2 and P3 indicate Mg²⁺ concentration peaks. The y axis presents the height (cm w.e.) above the surface of the superimposed ice. The September 2003 superimposed ice height (0 as plotted here) remained constant until approximately mid-June 2004, when the height increased as new ice was added by refreezing of percolating meltwater. These profiles were selected from among the 54 that were created from the weekly sampling in order to illustrate seasonal changes.

Seasonal variations of dust, Mg²⁺ and Ca²⁺ in the surface snow

Dust and chemical species are removed from the atmosphere through dry and wet deposition (Reference Heather, Yi, Moumen, Han and HolsenHeather and others, 2004). For both types of deposition, precipitation and wind are the main control factors on UG1. Once aerosols accumulate on the glacier surface, they undergo post-depositional alteration, which is mainly influenced by temperature and meltwater percolation. Surface samples collected from the uppermost 1–5cm of surface snow were examined to investigate the chemical seasonality in precipitation and dry deposition (Fig. 3). The concentrations of all three species were low from October to the end of March, then were elevated from April to June. After that, they show different characteristics: Ca²⁺ rapidly decreased in June, but Mg²⁺ and, to a lesser extent, dust peaked along with August snowfall.

Fig. 3.

Seasonal changes in calcium, magnesium and insoluble particle concentrations in surface snow and daily variability of temperature, precipitation and the prevailing wind speed vs time from September 2003 to September 2004 recorded at the Daxigou meteorological station. Dates are mm/dd/yy.

Data from the Daxigou meteorological station (3539ma.s.l.), located 3km away from UG1, show that the atmospheric stability, temperature, local valley wind strength and the precipitation were related to the insoluble and soluble aerosol concentrations in the surface snow. This can be seen in Figure 3 where the peak in surface snow concentrations is associated with wind-speed peaks and the precipitation. The high concentrations between May and June may be attributed to the local valley wind, which could potentially cause more dust input into the atmosphere and result in increased Ca²⁺ and Mg²⁺ concentrations. The juxtaposition of high dust and Mg²⁺ concentrations in July and August 2004 may have been due to the transport of these species from remote areas by moisture advection, which suggests that the Mg²⁺ concentration in the surface snow may be related to the dust coming from these remote regions. In winter, the low concentrations coincide with the temperature inversions and stable atmospheric stratification, similar to conditions that are observed in the Alps (Reference Maupetit, Wagenbach, Weddeking and DelmasMaupetit and others, 1995; Reference Kuhn, Haslhofer, Nickus and SchellanderKuhn and others, 1998).

Possible sources of Ca²⁺ and Mg²⁺

The sources of the Ca²⁺ and Mg²⁺ in UG1 can be assessed by examining the correlation between various ions in the snow, as well as the atmospheric circulation pattern that brings moisture to the region. Based on the correlation matrix of ions captured from the surface snow at the site, we observe that the linear correlation of Ca²⁺ with electric conductivity and pH is 0.97 and 0.77, respectively (two-tailed, p = 0.01, N = 45). This indicates that the main components of the atmospheric dust are calcium-rich minerals, which probably come from the weathering of local rocks, as well as from the surrounding desert. Magnesium and dust are significantly correlated (R = 0.74) (two-tailed, p = 0.01, N = 45), which suggests that the Mg²⁺ source is more distant and may be mainly related to precipitation events.

Prevailing westerlies dominate the air circulation over the study area (Fig. 4), and westerly winds are especially dominant over the eastern Tien Shan when the circum-Arctic vortex is stronger (Reference Zhang and DengZhang and Deng, 1987; Reference Hu and JiangHu and Jiang, 1989; Reference QiuQiu, 1993; Reference Jiang, Zhu, Wei and AbeJiang and others, 2002). Therefore, moisture travels through this region from west to east. Along with this pattern of atmospheric circulation, the aerosols, which include Mg²⁺ and Ca²⁺, are blown from the inland deserts and transported to the study area by this strong airflow. This suggests that long-range transport accounts for part of the Ca²⁺ that is present in the snow pits.

Fig. 4.

Mean air-mass trajectory at 1500 m above the Tien Shan and surrounding areas during the spring season from 1960 to 1969 (modified from Reference LiLi, 1991). The location of the study site is indicated by the black circle. ‘A’ indicates anticyclone, ‘C’ indicates cyclone and the dashed line is national boundaries.

Summary

Long-term Mg²⁺, Ca²⁺ and microparticle data from snow pits were examined to determine the depositional and post-depositional processes that occur on UG1. During the winter, the formation of the vertical stratigraphy of the microparticle, Mg²⁺ and Ca²⁺ concentrations in the upper layers of the glacier was mainly related to snow compaction, sublimation and dry deposition. During the summer, the snow in the pit experienced the maximum post-depositional alteration through the percolation of the meltwater; however, alteration deeper in the snow pit was very slight and the general information was still preserved.

The seasonal changes in the concentrations of calcium and magnesium in surface snow display a characteristic sequence of low and high values. Low values of Ca²⁺ and Mg²⁺ were observed during the winter from November to April. The concentrations increased in May to several times those of the winter, peaked in June and then rapidly decreased through August. Through the autumn the concentrations appear to have been stable. The possible sources of Ca²⁺ may primarily be the local rocks and secondarily from a more remote source, while Mg²⁺ may be primarily from a remote source.