Introduction

Sediment yield, based on a monitoring programme of sediment transport in meltwater rivers, is often used to obtain the rate of erosion beneath a glacier. Such measurements in a number of glacier rivers in different regions have shown that suspended-sediment concentration in meltwater is highly variable at both short-term and seasonal time-scales. This variability has been related to availability of sediment supplied to the subgiacial channel system (Reference Østrem, Jopling and McDonaldØstrem, 1975), changes in the area that water is washing over during a flood event (Reference LiestolLiestøl, 1967) and exhaustion effects (Reference Gurnell, Gurnell and ClarkGurnell, 1987; Reference Gurnell, Hudson, Clark, Bogen, Hasten and TranterGurnell and others, 1994). Reference CollinsCollins (1989) interprets the seasonal pattern of variation in sediment flux of meltwater from Gornergle-tscher as a seasonal development of the subgiacial drainage system. Throughout the season, areas of previously hydraulically isolated sub-sole are integrated with flow, releasing quantities of sediment from basal storage.

Sediment yields have been shown to be different for various types of glaciers. With some exceptions, large valley glaciers are characterized by large yields, and small cirque glaciers by low yields. Glaciers in different regions having different thermal regimes and on various bedrock types are also characterized by different yields (Reference Hallet, Hunter and BogenHallet and others, 1996).

Annual sediment yields of Norwegian glaciers (maximum 1300 t km⁻²) are, in general, lower than those of glaciers elsewhere. The sediment yield at Yaluajökull has been measured as 12kt km⁻² (Tomasson, 1987) and at Gornergletscher as 6 kt km⁻² (Reference BezingeBezinge, 1978). When the glacial erosion rate is high, a different pattern of sediment flux is expected from that produced by glaciers with small rates. Sediment yields of Norwegian glaciers are subject to variations from year to year. In some cases such variations may be of the same order as those between different glaciers. Glacial erosion is dependent on glacial quarrying and abrasion, processes that are unlikely to vary on time-scales shorter than decades. Thus, year-to-year variability in sediment yield has to be accounted for by other processes. This paper presents sediment yields for four glaciers in Norway and discusses reasons for the annual variations. Sediment yields are then translated into erosion rates.

Sediment yields are obtained by monitoring of water discharge and sediment transport in meltwater streams close to glacier outlets. Sediment samples were collected with ISCO automatic samplers programmed for four samples a day. Grain-size analyses of the suspended-sediment load were determined on large-volume samples collected on a weekly basis. Further descriptions of the methods are given by Reference Bogen and HasholtBogen (1986, Reference Bogen1988, Reference Bogen1992).

Sediment Yields

The glaciers studied are shown in Figure 1. Øvre Beiarbre is a small cirque glacier(2.4km²; see Table 1), situated in northern Norway, east of the Svartisen ice cap. Sediment transport has been monitored in its meltwater river since 1988. The sediment yield in 1988 was one of the highest on record among Norwegian glaciers at that time. The rate of 886 t km⁻² year⁻¹ has only been exceeded at nearby Trollbergdalsbreen (Reference Østrem, Jopling and McDonaldØstrem, 1975). The high yield did not last, and suspended-sediment delivery declined to 176 t km⁻² year⁻¹ in 1989, and 173 t km⁻² year⁻¹ in 1990. In 1991, however, the sediment yield exceeded the 1988 level, reaching 1136 t km⁻² year⁻¹ before falling to lower levels in 1992 and 1993 (Fig. 2). Thus, high year-to-year variability appears to be a characteristic feature of the sediment transport in the Beiarbreen meltwater river. As seen from the record of water discharge, the high yields are due to higher concentrations of sediments and not to larger runoff in these years.

Fig. 1.

Location of glaciers in Norway included in this study.

Table 1.

Area, mean sediment yield and mean erosion rates of the investigated glaciers

Fig. 2.

Annual sediment yield, g_s, (solid columns) and runoff, Q, (grey) from Øvre Beiarbre during the years 1988-93.

It is difficult to relate the high yields to glaciological variables. The glacier is thin and slow-moving, and is apparently unable to erode these high rates in its present state. For this reason, Reference Østrem, Jopling and McDonaldØstrem (1975) attributed the high yields of Trollbergdalsbreen to supply from sediments eroded during a former, more active phase. To illustrate further the sudden change in sediment concentration, a regression analysis of concentration vs water discharge was carried out for a year of high yields (1991) and one of low yields (1990). Significant correlations were found for each year (Fig. 3). However, an analysis of the combined data for both years resulted in a lower coefficient of correlation, indicating two different populations. This phenomenon may be due to a shift in sediment sources, possibly caused by a change in the position of the subgiacial conduits.

Fig. 3.

Regression analysis of suspended-sediment concentration, C_s vs discharge, Q, in the meltwater river from Øver Beiarbre. Coefficient of correlation on data from 1990, r = 0.67 and 1991, r = 0.73. An analysis including both years gave r = 0.36.

The valley glacier Nigardsbreen (48.2 km²), an outlet from the Jostedalsbre ice cap, shows a similar variability. The year-to-year variations are not as large as for Øvre Beiarbre. However, there is no significant correlation between water discharge and sediment concentration on an annual basis (Figs 4 and 5). In addition, the range of concentration is narrower than at Øvre Beiarbre, and no concentrations lower than 0.010 g l⁻¹ were observed.

Fig. 4.

Annual sediment yield, g_s, (solid columns) and runoff, Q, (grey) of Nigardsbreen during the years 1987–93.

Fig. 5.

Regression analysis of suspended-sediment concentration, C_s vs water discharge, Q, in the meltwater river from Nigardsbreen. Coefficients of correlation of the three years 1989, 1990 and 1993 are r = 0.36, 0.56 and 0.70, respectively. Analysis of all years together gives r = 0.55.

A similar pattern is observed at Engabreen (36.2 km²), a western outlet glacier of the Svartisen ice cap (Fig. 6). The correlations were as low as 0.30 in 1990, when the yield was high, increasing to 0.6 in 1992, a year of lower yield (Fig. 6).

Fig. 6.

Annual sediment yield, g_s, (solid columns) and runoff, Q, (grey) from Engabreen during the years 1987–93. No measurements were made in 1988.

The pattern of variability in sediment yield for these glaciers may be interpreted in terms of a model where the sediments are introduced to the subgiacial waterways by melting of debris-rich ice in the glacier sole (Fig. 7). The rate of deformation of conduits depends on the difference between the ice overburden pressure and the internal water pressure. Due to variations in glacier melting and precipitation, water discharge in the subglacial conduits is subject to changes throughout the season. In periods of low water discharge, the movement of the glacier and the plastic deformation of the ice will deform the conduits. A subsequent expansion by an increase in water pressure will melt more ice and add more sediments to the subgiacial system. In a system of equilibrium conduits, the dominant sediment sources are the beds of the conduits and possible subgiacial till. Such sources should be expected to give a good relation between sediment load and discharge, but that is not true for the glaciers included in this study. The pattern of sediment transport in the meltwater rivers of the glaciers is availability-controlled. That is, the rate of increase in discharge does not always give the same rate of increase in sediment load, depending on whether sediments are available for transport. This pattern, along with the low erosion rate, strongly suggests that subgiacial till is not the dominant source. Most probably, the glacier soles are resting on bedrock on which till is only present in patches. In such systems, fluctuations in water pressure and glacier flow rate are as important as total runoff in controlling the acquisition of sediment.

Fig. 7.

Schematic diagram indicating the way that a cavity or an ice tunnel melts out sediments incorporated in the ice. (a, b) Water pressure is rising and the subgiacial cavity is expanding. (c) Water pressure is falling and the tunnel or cavity is deformed. (d) Changes in the position of the drainage system may increase availability of sediments.

It is likely that thick, fast-moving glaciers such as Nigardsbreen and Engabreen will deform their empty subgiacial conduits at a more rapid rate than the thin, slow-moving Øvre Beiarbre. Water from the subgiacial conduits of Engabreen is used for hydroelectric purposes, and water is collected beneath the glacier. Engabreen is 200 m thick in the area of the subgiacial water intake. Inspection tunnels melted out beneath the ice are subject to substantial deformation in the course of 3–4 days. The poor correlation between water discharge and sediment concentration suggests that such deformation of the conduits takes place continously throughout the season. This process is more rapid at Engabreen than at Øvre Beiarbre. At the water intake, the lowest part of the ice consists of a debris-rich sole 1-2 m thick, moving over a mostly bare rock bed. The bedrock areas are no source of sediments for the subglacial waterways. However, pockets of subglacial till may exist outside the investigated areas.

Channels do not necessarily form in the same position each year. There are several intakes beneath Engabreen, and the position of the active intake shifted between 1993 and 1994. The somewhat larger yearly variability of the Engabreen record compared to Nigardsbreen may be attributed to more frequent shifts in channel positions to areas that may have different concentrations of debris in basal ice.

Beneath the thin, slow-moving Øvre Beiarbre, conduits do not defrom at the same rate as beneath the two other glaciers. The basal ice along the subglacial drainage system may after some time be washed clear of sediments. Deformation of the conduits to allow for more melting of debris-laden ice will take a longer lime. In some years, there is a large shift in sediment yield, but such a shift does not necessarily take place every year. Most probably, a year with high yield is preceded by a winter deformation causing a major change in the position of the conduits or linked-cavity systems to areas of ice richer in sediment. In some years the sediment yield remains low, presumably because no change in position took place.

Brøggerbreen is a sub-polar glacier, located near Ny Ålesund in Svalbard. Year-to-year variability in sediment yield is high, as shown in Figure 8. Sediment loads have been found to be correlated with water discharge (Reference ReppRepp, 1978, 1985; Reference BogenBogen, 1989, Reference Bogen, Gjessing, Hagen, Hassel, Sand and Wold1991), but in recent years this correlation has been weak.

Fig. 8.

Annual sediment yield, g_s, (solid columns) and runoff, Q, (grey) of Breggerbrem 1989–93.

The sediment-monitoring station is situated about 1 km downstream from the glacier snout. Some erosion of moraine material and formerly deposited sediments along river-banks takes place. Thus, the sediment yield may also be influenced by processes in the proglacial reach of the channel.

Discussion and Conclusions

The pattern of yearly variability of erosion rates indicated by sediment yields is different for the four glaciers included in this study. The small, thin Øvre Beiarbre is characterized by years of excessively high sediment yield being interspersed with low-yield periods of at least 2 years. It is suggested that this pattern is associated with sediment-exhaustion effects that last for some years, followed by channel changes that increase sediment availability.

The relatively thick and fast-moving valley glaciers Engabreen and Nigardsbreen seem to maintain sediment availability by deformation of their subglacial conduits and subsequent melt-out of sediments when the water level rises again. Much sediment is washed out from these glaciers in summers when water pressure is subject to frequent fluctuations.

The dependency of sediment yield on water discharge for the sub-polar Brøggerbreen during some years indicates a system of conduits that rarely change their position from year to year. However, in other years channel changes may take place, making more sediment available. A significant part of the sediment load may be eroded from subaerial locations.

Glacial quarrying and abrasion convey a continuous supply of debris to the glacier sole. The sediment yield of glaciers is dependent on the concentration of debris at the sole and, at least for the temperate glaciers included in this study, there is a clear relation to glacial erosion rate.

However, the melt-out processes that remove debris from the sole operate on a much shorter time-scale than glacier erosion. In order to use records of sediment yield in meltwater to estimate erosion rates, several years of data should be used to even out variability originating from melt-out processes. Average values are then the most meaningful indicators of long-term bedrock erosion rates (Table 1).

It is interesting to compare the present rate of erosion of Engabreen (0.168 mm year⁻¹) with the rate obtained by Reference RekstadRekstad (1912). Rekstad estimated a rate of 11 mm year⁻¹ from the infill of a small lake in front of the glacier. At that time, the snout of the glacier most probably rested on old lake sediments deposited in lake Engabrevatn prior to the glacier advance of the 18th century. Despite the difference in methods, it may be concluded that glacial erosion of a soft bed beneath this glacier takes place at a rate that is at least one order of magnitude larger than that of bedrock.