Introduction

Glacial environments are often considered as areas of low chemical weathering rates, due to low temperatures and minimal biological activity (Kump and Alley, 1994). This conviction has been used to justify assumptions of minimal chemical weathering beneath ire (Gibbs and Kump, 1994; Kump and Alley, 1994). Recent empirical, hydrochemical work shows temperate glaciers to be characterised by elevated chemical weathering rates, as much as 1.2–2.6 times the continental average (Souchez and Lemmens, 1987). The supply of large volumes of dilute meltwaters to highly reactive, freshly comminuted, glacial rock flour and other glacial debris facilitates rapid rates of hydrolytic weathering of carbonate and aluminosilicate rocks. These reactions usually require a supply of protons. This condition is partly satisfied by carbonation reactions, involving the dissociation of ction in pCO₂ and consequent diffusion of CO₂ into solution. This may take ring also provides a mechanism whereby CO₂ is drawn down from the atmosphere with increasing demand for protons (Sharp and others, 1995).

Current assessments of glacial chemical weathering rates are derivarbonic acid derived from the dissolution of CO₂ in water. Consumption of protons increases the pH of a solution, lplace wherever waters come into contact with the atmosphere via open conduits or air bubbles in the ice. Thus, chemical weatheeading to a reduced from temperate glaciers, where meltwater has considerable contact with basal rock material via a well-developed subglacial drainage system (Sharp and others, 1995). Chemical weathering beneath high-Arctic glaciers, however, has received comparatively little attention. A pre-dominance of cold basal ice on these glaciers is held to restrict the access of meltwaters to the bed (Sugden and John, 1976), leading to low overall chemical weathering rates. Support for this argument derives from the only two chemical weathering rates measured on high-Arctic glaciers, of 160 meq ¬⁺ m⁻² year⁻¹ at Scott Turnerbreen in central Spitsbergen (Hodgkins and others, in press) and ~110 meq ¬⁺ m⁻² year⁻¹ at Austre Brøggerbreen, Svalbard (A. J. Hodson, unpublished data), where meltwater contact with glacial debris is restricted to supraglacial and ice-marginal environments.

Most glaciers on Svalbard are polythermal (Dowdeswell and others, 1984) with at least part of their basal ice at the pressure-melting point (Schytt, 1969). Chemical weathering rates in these glacial systems have yet to be evaluated. Here, we address this shortcoming through an investigation of runoff and hydrochemistry at Finsterwalderbreen, a polythermal glacier in southern Spitsbergen.

Study Area And Methods

Finsterwalderbreen (77°28ʹ N, 15°18ʹ E) has a catchment area of 68 km², of which 44 km² is glaciated (including 9 km² of dead ice) (see Fig. 1). The glacier is 11 km long and has a polythermal regime, being mainly warm-based except beneath the thinner ice at the front and lateral margins (èdegård and others, 1997). The equilibrium line is located in a zone around 500 m a.s.l. (personal communication from J. F. Pinglot and others, 1996). The glacier is reported to have surged some time between 1898 and 1910, during which its lower half increased in thickness (Nuttall and others, 1997). The bedrock geology is mainly of sedimentary origin, consisting of Precambrian carbonates, phyllite and quartzite, and Permian sandstones, dolomites and limestones in the upper catchment, and Triassic to Cretaceous siltstoncs, sandstones and shales at lower elevations (Dallmann and others, 1990).

Fieldwork was conducted during the 1994 and 1995 melt seasons from 24 June to 19 August (Julian days 176–231) and 25 June to 14 August (Julian days 176–227), respectively. About 90% of the glacier’s meltwater drains from two outflows on the western margin: a basal conduit and a subterranean upwelling of water about 10 m to the east of the basal conduit (Fig. 1). These two outflows converge 10 m downstream and together constitute the bulk meltwaters. A gauging station was established approximately 10–40 m downstream from the confluence. Frequent channel migration, high flows and icebergs periodically destroyed the gauging station, which was subsequently repositioned at the nearest convenient site. Bulk meltwater stage was measured continuously by a Druck pressure transducer, and hourly averages of 10 s readings were logged by a CR10 data logger. Stage was calibrated to discharge daily by manual gauging when possible, using the velocity/area method (Tranter and others, 1996). Diurnal variations in discharge were considered insufficient to warrant more frequent calibrations. Errors in discharge data are ~15%.

A single bulk meltwater sample was collected daily between 1500 and 1900 h throughout both the 1994 and 1995 melt seasons. Samples were filtered immediately and stored in plastic bottles. The samples were analyzed for pH using a portable Orion 290A pH meter and Orion pH electrode up to a few days after storage. Cl, and Ca²⁻ were determined by ion chromatography on a Dionex 4000i some 2–9 months after collection. Alkalinity (predominantly ) was determined by colorimetric titration up to 2 months after collection. The precision of these determinations is ±4% and ±0.6%, respectively. The mean charge balance error for bulk meltwaters was −2.7%.

During spring 1995, 60 snow samples were collected from six pits located along the glacier centre line, so that bulk meltwater solute concentrations could be corrected for snowpack input. Within 24 h of collection, snow samples were melted, filtered and stored at room temperature for 2 weeks–4 months. Chemical analysis was carried out as above.

Results

Concentrations of Ca²⁺ were corrected for the sea-salt-derived contribution from the snowpack by using the ionic ratio of Cl: Ca²⁺ in sea water (Holland, 1978) and the Cl⁻ content of bulk runoff (assumed to be derived entirely from sea salt). concentrations in the bulk runoff were also corrected for the snowpack input (i.e. that associated with sea salt and with other containing aerosols) using the mean ratio of Cl: in snow samples. Non-sea-salt Ca²⁺ and non-snowpack are denoted as “*”.

Discharge time series for both the 1994 and 1995 field seasons are given in figure 2a. Both seasons exhibit mid-season peak flows, with periods of recession during the early and late season, when discharges were < 6 m³ s⁻¹ in 1994 and <2 m³ s⁻¹ in 1995. High flows towards the end of 1995 (JD 224) are probably associated with accelerated ablation and rapid transit of meltwater through an efficient, well-developed, channelised drainage system. The peak discharge is up to three times greater during 1994 than 1995 due to high rainfall, attaining values of 35 m³ s⁻¹. loads replicate the main trends in discharge, with the highest loads registered during peak flows (Fig. 2b). and Ca²⁻ loads also display similar trends, although these data are not presented here.

Fig. 1.

(a) Sketch map of glacier snout, (b) Map of Finsterwalderbreen, Svalbard.

Rates of chemical weathering were calculated in the following manner. The errors in flux determinations, estimated to be ~ ± 25%, are similar in magnitude to those in previous chemical weathering studies. Solute fluxes have not been corrected for rainfall inputs of non-sea-salt aerosol, which are considered to be relatively trivial. The annual water flux for 1994 and 1995 was determined by calculating the flux of water per hour, and summing the values for the whole season. Missing discharge values were interpolated, or predicted from the association between electrical conductivity and discharge for the preceding and following periods. The cumulative water flux for the season was multiplied by the summed discharge-weighted mean concentration of HCO₃ and ^*SO₄^2– (assumed to be equal to the cation concentration by charge balance). This value was then divided by the catchment area (68 km²) to give the rate of chemical weathering over the sampling season in meq Σ⁺ m⁻². We estimate that ~80% of the annual bulk runoff was discharged during the sampling season (after Repp, 1988). Given that our gauging site collects ~90% of the drainage from the catchment, the total water flux measured is ~72% of the annual flux. Rates of measured chemical weathering and water fluxes are given in Table 1, as are our estimated annual rates.

Fig. 2.

Temporal variation in (a) bulk runoff (Q) and (b) loads during 1994 and 1995 at Finsterwalderbreen. Julian days 176–231.

The concentrations of crustal ions (HCO₃^– and *Ca²⁺) in bulk melt water samples show inverse relationships with discharge (Fig. 3a). Both ^*SO₄^2– and HCO₃ display high concentrations at low discharge (>700 (μeq 1⁻¹), but while ^*SO₄^2– declines steeply as discharge rises, the corresponding decrease in HCO₃ is less and concentrations of >400 μeq 1⁻¹ are maintained. The association of ^*Ca²⁺ (as the major cation) with discharge represents the summation of both these trends.

We have estimated the minimum CO₂ drawdown from instantaneous HCO₃^– loads, averaged over an hour, as follows. Of the total HCO₃, some is assumed to be derived from coupled sulphide oxidation/carbonate dissolution:coupled sulphide oxidation/carbonate dissolution

(1)

Hence, two moles of HCO₃^– for each mole of SO₄^2– are subtracted from the total concentration of HCO₃^–. Of the remaining HCO₃^–, half is assumed to come from the atmosphere and half from carbonate rocks:carbonation of carbonates

(2)

We have also applied a minor correction for HCO₃^– acquired by the neutralisation of snowpack acidity. These calculations give a minimum estimate of CO₂ drawdown, as they do not take account of HCO₃^– derived from the carbonation of aluminosilicate and silicate minerals.

CO₂ drawdown at Finsterwalderbreen ranges from 1 to 150 kg Ch⁻¹ and exhibits a strong direct association with bulk discharge (1.5 g C m⁻³, R ² = 0.96) (Fig. 3b). This compares with a rate of 1.2 g C m⁻³ drawdown at Haut Glacier d’Arolla, Switzerland (Sharp and others, 1995).

Table. 1.

Water fluxes and chemical weathering rates at Finsterwalderbreen

Discussion: Rates Of Chemical Weathering And Co₂ Drawdown

Fig. 3.

Association between and Ca²⁺ and bulk discharge in 1994. HCO₃^– data for 1995 are also included, (b) Association between bulk discharge and CO₂, drawdown in 1994 and 1995.

Calculated chemical weathering rates of 440 and 210 meq Σ⁺ m⁻² year⁻¹ in 1994 and 1995, respectively, (see Table 1) give a mean annual weathering rate of 330 meq Σ⁺ m⁻² year⁻¹. These rates are considerably higher than rates of ~ 110–160 meq Σ⁺ m⁻² year⁻¹ measured at predominantly cold-based glaciers (Hodgkins and others, in press; A. J. Hodson, unpublished data), and approach chemical weathering rates on temperate glaciers that range from 450 to 1000 meq Σ⁺ m⁻² year⁻¹ (see Fig. 4). Inter-glacier comparisons of chemical weathering rates, however, are complicated by a number of factors. There may be error in some of the former estimates due to the failure to distinguish between crustal and atmospherically derived solute (Sharp and others, 1995). Varying degrees of glacierization of the catchment area, together with differing relative proportions of active and stagnant ice, may also influence the magnitude of calculated chemical weathering rates. For example, chemical weathering rates at Kinsterwalderbreen are considerably deflated because only half of the catchment is occupied by active glacier ice. We also appreciate that differences in lithology confound a simple, direct comparison between basins. Since an appreciable quantity of reactive carbonate minerals exists in the upper catchment of Finsterwalderbreen, the chemical weathering rates we calculate may be higher than for basins that do not contain carbonate rocks. Chemical weathering rates at Finsterwalderbreen, however, are 2–3 times the magnitude of those calculated for Brøggerbreen, Svalbard (A. J. Hodson, unpublished data), a predominantly cold-based catchment of similar lithology. This points towards thermal regime as a first-order control on chemical weathering rates. Extrapolation of our findings to other high-Arctic polythermal glaciers leads us to conclude that these ice masses may make a more significant contribution to global chemical-weathering budgets than previously assumed, since the rates are similar in magnitude to the continental average of 390 meq Σ⁺ m⁻² year⁻¹ (Livingstone, 1963).

Discharge exerts a strong control on solute fluxes at Finsterwalderbreen, as illustrated by seasonal trends in HCO₃^– loads and bulk runoff during 1994 and 1995 (Fig. 2b). The higher HCO₃ loads in 1994 than in 1995 show that high discharges arc accompanied by elevated solute fluxes. This supports conclusions reached in Alpine studies of chemical weathering rates and reflects the high flushing rates, turbulent meltwaters and high suspended-sediment concentrations which accompany high discharges (Sharp and others, 1995). These factors serve to promote chemical weathering by preventing the equilibration of meltwaters, providing large quantities of weatherable material and facilitating diffusion of CO₂ into solution.

The strong interannual variability in chemical weathering rates at Finsterwalderbreen can also be ascribed to contrasting discharge conditions over the two melt seasons (Fig. 2a). A high incidence of intense rainfall events during the 1994 sampling season (~79mm) was responsible for elevated discharges (>35 m³ s^−l), producing a measured water flux of 4.1 × 10⁷ m³. This compares with only 1.7 × 10⁷ m³ in 1995 when rainfall receipts were ~27 mm over the melt season and net incoming solar radiation exerted a stronger control on meltwater generation. It should be noted that these rainfall amounts were measured at sea level, and that precipitation at higher elevations in the catchment probably fell as snow and therefore did not contribute directly to runoff. Thus, meteorological conditions are an important determinant of chemical weathering rates via elevated discharge. High interannual variability in discharge, and hence chemical weathering rates, may be the norm on Spitsbergen glaciers (Repp, 1988). The 1994 and 1995 melt seasons represent extremes of rainfall conditions, the typical incidence of rainfall during summer in Spitsbergen lying intermediate between those recorded in 1994 and 1995 (unpublished information from Norsk Polarinstitutt, Oslo). Annual weathering rates of 440–210 meq Σ⁺ m⁻² year⁻¹ are, therefore, probably more common.

The incidence of elevated chemical weathering rates at Finsterwalderbreen, relative to cold-based glaciers, has implications for the drawdown of CO₂ from the atmosphere. The steeper decline in ^*SO₄^2– with discharge, relative to HCO₃ (Fig. 3a), signifies an increasing dominance of carbonation reactions over sulphide oxidation as discharge rises, and an increased drawdown of CO₂ into solution. This increased relative contribution of carbonation maintains high fluxes of cations, as is evident from the behaviour of Ca²⁻ concentrations as discharge rises (Fig. 3a). These features explain the strong, direct association of CO₂ drawdown with discharge (Fig. 3b). The amount of CO₂ drawdown per unit of discharge (1.5 g C m⁻³) is higher than that reported at Haut Glacier d’Arolla, a temperate glacier in Switzerland (Sharp and others, 1995). This demonstrates the potentially important role played by polythermal glaciers in the drawdown of CO₂ from the atmosphere and the strong control of discharge on the magnitude of this removal. It is possible that periods of high meltwater production on longer time-scales, e.g. during deglaciation (Tranter, 1996) and the final stages of a surge, are accompanied by the removal of considerable volumes of CO₂ from the atmosphere, provided meltwater is able to access weatherable rock material.

Fig. 4.

Chemical weathering rates measured on glaciers of different thermal regime.

Conclusions

Chemical weathering rates at Finsterwalderbreen far exceed those measured on cold-based Arctic glaciers, and approach rates characteristic of temperate glacier systems. We consider thermal regime to be a first-order control on the magnitude of chemical weathering rates. A predominance of warm basal ice permits the development of a subgiacial drainage system beneath Finsterwalderbreen, allowing surface meltwaters to access reactive basal material and acquire solute. Extrapolation of these findings to other large, polythermal-based, high-Arctic glaciers leads us to conclude that these ice masses have high chemical weathering potential, particularly during high-runoff years. This has implications for the drawdown of CO₂ from the atmosphere at high discharges. The magnitude of CO₂ drawdown per unit discharge at Finsterwalderbreen (1.5 g Cm⁻³) is greater than that reported in the Alps (1.2 g C m⁻³; Sharp and others, 1995). We conclude that glacier basal thermal regime is an important determinant of chemical weathering rates through the degree of subgiacial routing of water. Consequently, high-Arctic regions cannot be considered as areas of low chemical weathering rates and CO₂ drawdown.