2.1.Introduction

Measurements of the concentration of deuterium, oxygen-18 and tritium in samples of snow, ice and stream water from a glacierized catchment area have already been used in previous studies for determining the shares of melt water from snow, melt water from ice, and subglacial spring water, in the discharge of a glacier stream during the summer ablation period (Reference Behrens, Behrens, Bergmann, Moser, Rauert, Stichler, Ambach, Eisner and PesslBehrens and others, 1971). This was possible, because of the low deuterium concentrations in spring water compared with those in melt water from snow and ice. Furthermore, melt water from old glacier ice contains no tritium at all. By measuring only deuterium and not tritium, it is not possible to distinguish between melt water from snow and ice during the summer ablation period, as the deuterium concentrations are approximately equal in both types of melt water. To distinguish between these two melt water contributions, the tritium concentrations must be measured additionally (Reference Ambach, Ambach, Eisner and UrlAmbach and others, 1973). In general, simultaneous measurements of deuterium and oxygen-18 concentrations give no further information on the proportions of melt water and spring water in a glacier stream.

The wide range of variations in deuterturn concentrations that occur in every individual precipitation is reduced considerably by metamorphosis of the snow cover and by mixing processes in the run-off system of glaciers. The final values obtained for melt water, stream water and spring water are mean deuterium concentrations with small ranges of variation of the respective samples, but significant differences, from which the relative shares of melt water and spring water in the total run-off of the glacier stream can be determined for a summer ablation period.

In the present paper the changes in isotope content from precipitation to run-off, and the related glacier-hydrological effects are discussed.

2.2.Isotope Content in the Precipitation and in the Snow Cover

Figure 2 shows the deuterium contentFootnote * in the samples taken from individual precipitation events at Vent ( Fig.1). The values plotted as a step function (solid line) are weighted monthly mean values of the deuterium content in the precipitations. The diagram shows on the one hand the typical annual variations with high values in the summer and low values in the winter, on the other hand the great fluctuations between successive precipitation events having the wide range of annual fluctuations. The variations in the isotope content observed during one individual precipitation event are almost as high as the annual variations (Reference Ehhalt, Ehhalt, Knott, Nagel and VogelEhhalt and others, 1963; Reference Bleeker, Bleeker, Dansgaard and LablansBleeker and others, 1966; Reference Ambach, Ambach von, Elsässer, Moser, Rauert, Stichler and TrimbornAmbach and others, 1975).

The individual layers of the winter snow cover can in general be well correlated to the mean isotope contents of successive periods of precipitation (Reference Moser and StichlerMoser and Stichler, 1975). In general, the snow surface shows enrichment of heavy isotopes, deuterium and oxygen-18 caused by fractionation processes during phase transitions (Reference Judy, Judy, Meiman and FriedmanJudy and others, 1970; Reference Moser and StichlerMoser and Stichler, 1970; Reference Moser and StichlerMoserand Stichler, 1975).

2.3.Range of Variation of Isotope Contents in samples of snow, ice and water from a glaciated catchment area as exemplified at Hintereisferner

Fig.2.

Seasonal fluctuations of the deuterium concentration at Vent (cf. Fig. 1).

(a) Precipitation, Vent: dots correspond to individual precipitations, the step function giving the weighted monthly mean value;

(b) Water samples Rofenache (RA), Vent: dots correspond to individual samples, the step function giving the unweighted monthly mean value.

The double standard deviation of the δD values is 1% ₀).

Figure 3 shows individual measurements of the deuterium content in samples of snow, snow-melt water, ice, ice-melt water, spring water and stream water taken during the ablation periods of 1969, 1970 and 1971. They show clearly a decrease in the range of variation from the snow samples (—45%₀ to — 160%₀) followed by the ice samples (— 90%₀ to —125%₀), the ice-melt water samples (—90%₀ to — 110%₀) and the creek samples (— 100%₀ to — 115% ₀) (Table II). This homogenization doubtlessly is largely due to mixing in the drainage system of the glacier. Processes of fractionation between percolating melt water and firn also cause homogenization accompanied by an enrichment of heavy isotopes. This has been shown earlier on drill cores from the accumulation area of Kesselwandferner in which homogenization of the ¹⁸O content was clearly observed in depths between 8 m and 15 m, the maximum depth of drilling (Reference Ambach, Ambach, Eisner and PesslAmbach and others, 1972). Although the percolation of melt water during several months hardly changes the profile of isotope content of a snow cover (Reference Moser and StichlerMoser and Stichler, 1975), long-term percolation of a firn layer must be assumed to have a homogenizing effect on the profile of isotope content.

The difference between the mean value of the deuterium content in spring water and that of snow and ice samples may be caused by fractionation processes during ice formation, but also by preferred alimentation of the springs by melt water from winter precipitation with low deuterium concentration. The mean value of the deuterium content of the glacier run-off, being a mixture of melt water and spring water, lies between the deuterium concentrations of the two run-off components. Furthermore it may be seen that the range of variation in deuterium contents of the spring waters is small and corresponds approximately to that of the samples of melt water from ice and stream water.

Fig.3.

Deuterium content of snow, melt weiter from snow, ice, melt water from ice, spring water and stream water of Hintereisferner. The samples were taken in July, August, and September of 1969 to 1971.

Table II.

Range of variation and mean values of the deuterium contents of samples from snow, melt water from snow, ice, melt water from ice, spring water and stream water of hintereisferner

The samples of snow, melt water from snow, ice, melt water from ice were collected in the summer months of the years 1969 to 1971, samples of spring water and stream water were collected July to September 1969-74.

2.4.Annual variations of the deuterium content in the run-off from three glaciers and in the Rofenache

Figures 4-6 show the variation of the deuterium content of individual samples taken over a period of several years from the glacier streams of Kesselwandferner, Hintereisferner and Vernagtferner in the catchment area of Rofenache and from Rofenache at Vent. For comparison, Figure 7 gives the corresponding variations for the spring at Hochjochhospiz (HJH) from the same catchment area.

At the beginning of the melting period (April to June), the deuterium content drops considerably down to a minimum (Figs 4-6). This is due to the direct run-off of melt water from snow layers located in the lower region of the glaciated catchment area as well as in the non-glacierized catchment area, the snow being accumulated during the winter at low temperatures, thus showing low deuterium concentrations. Shifts of the negative peak in the deuterium concentration depend on the ablation conditions in the months of April to June. The occurrence of such a negative peak in the graph for the Hochjochhospiz spring shows that this spring also contains a considerable share of melt water from winter precipitation running off directly during this period ( Fig.7).

Fig.4.

Seasonal variation of the deuterium content δD in the run-off of Hintereisfener (HEB) and Kesselwandferner (KWB) in the years 1966 to 1973.

Fig.5.

Seasonal variation of the deuterium content δD in the run-off of Hintereisferner (HEB) and Vernagtferner (VB) in the years 1971 to 1974.

Fig.6.

Seasonal variation of the deuterium content δD in the run-off of Hintereisferner (HEB) and Rofenache (RA) in the years 1969 to 1974.

Fig.7.

Seasonal variation of the deuterium content δD in the run-off of Hintereisferner (HEB) and the spring of Hochjochhospiz (HJH)for 1969 to 1974.

In the summer ablation period (July to September), the variation in deuterium content in glacier streams is governed by the different deuterium contents of the individual run-off shares (melt water from snow and ice, and subglacial spring water, Reference Behrens, Behrens, Bergmann, Moser, Rauert, Stichler, Ambach, Eisner and PesslBehrens and others, 1971), The deuterium contents of the glacier streams as well as those of the Hochjochhospiz spring increase during this period. This increase in the glacier streams on the whole is due to the run-off of isotopically heavy melt water from the ablation area, whereas in the case of the Hochjochhospiz spring the ground water discharge is superimposed on direct precipitation discharge.

During the winter accumulation period the variations are only small—in the glacier streams as well as in the Hochjochhospiz spring.

Comparing the deuterium content of the three glacier streams and Rofenache wc find annual variations of the same kind. The δD values of the Hintereisferner run-off, however, are somewhat higher, though parallel to those of Kesselwandferner and Vernagtferner. This is due to the different altitudes of the catchment areas. Figure 8 shows the distribution in altitude of the areas of the three glaciers. Table I gives some characteristic data: the altitude distribution of Hintereisferner significantly differs from that of Kesselwandferner and Vernagtferner.

Table III reviews the mean deuterium contents during the three run-off periods of winter, spring and summer for the three glaciers and for Rofenache. The limits of the individual periods were determined by the following conditions: the spring period (or summer period) shows the deuterium concentrations of individual samples to be smaller (higher) than the mean value of the winter run-off of the respective year (decrease in the deuterium content in spring is caused by the snow melt; increase in the summer is due to ice ablation, cf. Figs 4-6).

Fig.8.

Altitude distribution of the glacier area for Hintereisferner [HEF), Vernagtferner (VF) and Kesselwandferner (KWF) and the altitude of the averaged equilibrium tine. Right: fraction of glacier area per 50 m altitude interval. Left: integrated altitude distribution curve. The results for Hintereisferner and Vernagtferner were taken from Reference ReinwarthReinwarth (1972), results for Kesselwandferner were kindly made available by H. Hoinkes.

Table III.

Mean values of the dueuterium content (δD) In the run-off of hintereisferner (HEB), vernagtferner (VB), kesselwandferner (KWB) and the spring hochjochhospiz (HJH), as well as rofenache (RA) in the winter, spring and summer periods (COLUMN)

For an explanation of the time limitation of the seasons see text. In HJH, the winter covers a period from November to March, spring from April to June, summer July to September. Wherever possible, the differences in the mean deuterium contents △ΔD (of VB, KWB, HJH and RA) as compared to HEB are given.

The mean values of deuterium contents given in Table III are about 10.5%₀ and 901%₀ lower for the winter run-off of Vernagtferner and Kesselwandferner, respectively, than are the values for the winter run-off of Hintereisferner. For the summer ablation period, the corresponding values are 7.7%₀ and 7.1%₀ respectively. Comparing successive years, the mean deuterium concentration differs significantly for the snow-melt period in spring, the mean values of the deuterium concentration of Vernagtferner being especially low.

From the significant parallel shift in the graphs for annual fluctuations of deuterium content in glacier run-off (Figs 4-6) conclusions are made as to differences in the mean altitudes of the catchment areas using the isotope altitude effect. In view of an isotope altitude effect in precipitation of about — 3%₀ per 100 m (cf. Reference Moser and StichlerMoser and Stichler, 1970), the conclusion follows that the catchment areas of the winter discharge of Vernagtferner and Kesselwandferner on average are about 300 m higher than that of Hintereisferner. The difference in altitude calculated for the summer discharge is only about 250 m. The corresponding catchment areas of Vernagtferner are somewhat higher than those of Kesselwand ferner. Under the same assumptions, the isotope altitude effects of Rofenache and of Hintereisferner indicate that the mean total catchment area of Rofenache in the winter is about 150 m higher than that of Hinlereisferner. During the summer ablation period this difference in altitude is reduced by 50%.

The fact that the altitude of the catchment area of Rofenache was found to be higher for the winter run-off and the summer run-off than the catchment area of Hinlereisferner confirms the high contribution of Kesselwandferner and Vcrnagtferner run-off in the discharge of Rofenache. Due to local variations and variations in time of the altitude effect as well as to differences in deuterium data of successive years (Table III), the results on the altitude differences in catchment areas are not definite. However, the differences in the mean altitudes of glacier areas of Table I are smaller than those for the entire catchment areas obtained from the isotope analysis.

Table IV.

Time sequence of melt water contributions in the run-off of rofenache based on the seasonal fluctuations in deuterium content

Fig.9.

Daily variations of the deuterium content δD and the discharge of Vernagtferner (VB) for the period from 30 August 1974 to 6 September 1974. Data on discharge were kindly made available by O. Reinwarth.

On account of the highly glacierized catchment area, the seasonal changes in deuterium content of Rofenache.( Fig.6) are similar to those of the individual glacier run-off. The δD values of the individual samples from Rofenache vary between — 100%₀ and — 130%₀, the monthly means being between —105% ₀ and — 125%₀. Remarkable is the highly constant isotope content which is repeatedly observed in the winter run-off. The mean values for the winter months of 1973 and 1974 are — 112.0% ₀ and — 112 1%₀, respectively. The fluctuations in δD values of Rofenache characterize very well the onset of snow ablation by a drop in deuterium content. The transition from ablation of winter snow to ice ablation is marked by an increase in δD values. The beginning of winter run-off is characterized by an approximately constant deuterium content. In Table IV, the time sequence of these characteristic run-off periods is reviewed for the years 1972-74. The values were obtained from the variations in deuterium concentration. The relation between the daily variations of deuterium content and the discharge observed for Hintereisbach during a mid-summer ablation period by Reference Behrens, Behrens, Bergmann, Moser, Rauert, Stichler, Ambach, Eisner and PesslBehrens and others (1971) was confirmed. As a further example, Figure g shows the variations in deuterium content of Vernagtbach during eight days of measurements. Evidently, the deuterium content increases and decreases in phase with discharge. This confirms the result that the melt-water How on the glacier surface during periods of high ablation rate directly from the glacier surface contains more deuterium than the base flow. However, the high δD values on 5/6 September 1974 are due to melt water from a thin snow cover (snow fallen during the night of 3 to 4 September 1974), which melted with a delay because of the cool weather on 4 September 1974.

2.5.Mean proportions of melt water running off directly and of spring water in the discharge of Hintereisferner for the months of July to September

Table II contains the mean deuterium concentrations of stream water, spring water, ice-melt water and snow-melt water, and also of ice samples and snow samples. The individual values of the years 1969-71 are presented in Figure 3. From it, the following characteristics are obtained:

The variation in the δD values of snow samples is very wide, varying between — 50%₀ and — 160%₀.

The mean value of the deuterium concentration of —98.8%₀ in the group of snow plus snow-melt water samples is very close to that of the group of ice plus ice-melt water samples (— 100.7%₀). Hence it follows that it is not possible to distinguish between ice-melt water and snow-melt water during the summer months by measuring the deuterium content.

The mean values of deuterium concentrations of spring water, melt water (from ice and snow) and stream water differ significantly, showing small ranges of variation of the respective examples. It is therefore possible to calculate the discharge contributions of melt water and spring water in the total discharge from the deuterium concentrations of stream water.

For calculating the discharge shares of melt water and spring water in the total discharge, the following values were used from Table II:

Mean deuterium concentration of stream water for the months of July to September; — 106.6%₀).

Mean deuterium concentration of spring water: — 116.0%₀.

Mean deuterium concentration of melt water: —100.7%₀.

From these data the mean contribution of melt water to the Hintereisferner discharge was found to be 60% and that of spring water 40%. Thereby it was assumed that the δD values of the base How are equal to those of the spring water during the sampling period. The result obtained by averaging the δD values over the months of July to September is in good agreement with the contributions determined for individual days of the ablation period by Reference Behrens, Behrens, Bergmann, Moser, Rauert, Stichler, Ambach, Eisner and PesslBehrens and others (1971). Measuring the tritium concentration in the midsummer ablation period, Reference Ambach, Ambach, Eisner and UrlAmbach and others (1973) also found the proportion of melt water from the ablation area of Kesselwandferner to be 31% during the night hours and 57% during day-time as minimum and maximum values, respectively. Melt water from snow was not considered in these values.

The assumption that the mean δD value for melt water is — 100.7%₀ is explained as follows: Table II shows that the mean values of the deuterium concentrations in the samples of snow, snow-melt water, ice, and ice-melt water are not significantly different. Because of the small range of variation in δD values of the group of ice plus ice-melt water samples, this value appears as being better supported than the value of the group of snow plus snow-melt water samples. It thus seems to be justified that the δD value of the group ice plus ice-melt water samples may be taken for that of melt water, irrespective of its origin (ice or snow). It is easy to understand that the difference in the mean values of the groups of snow plus snow-melt water samples ( — 98.8%₀) and ice plus ice-melt water samples (—100.7%₀) is small, because the ablation area copies the accumulation area on account of rheological processes, the ice of the ablation area originates from precipitation deposited in the accumulation area. In the present case it cannot be proved statistically that the deuterium content in melt water from ice is higher than that in melt water from snow, although it is assumed that metamorphosis from snow into firn and secondly into ice must effect a change because of the fractionation processes mentioned in section 2.3. Deuterium concentration of snow-melt water differs significantly from that of ice-melt water only in special cases, e.g. if the melt water from new snow in summer occurs with high deuterium concentrations.

2.6.Time variation of tritium content in the discharge of Hintereisferner and in Rofenache

Fig.10.

Upper section: Seasonal variation of the tritium content in the run-off Hintereisferner (HEB; individual samples) and Rofenache (RA; unweighted monthly mean) in the years 1973 and 1974. The double standard deviation of the measured values is 9-13 T. U. at maximum. Middle section: Seasonal variations of the tritium content in precipitation samples. Vent, weighted monthly means. Bottom section: Monthly means of discharge of Rofenache (gauge at Vent). (The Hydrographischer Dienst, Innsbruck, is thanked for supplying the measured discharge data.)

Figure 10 shows the seasonal variations of tritium contents in the Hintereisferner discharge and in Rofenache. The curves have a shape similar to that of stream samples from the Rofenache catchment area published earlier (Reference Ambach, Ambach, Eisner and UrlAmbach and others. 1973; Reference Behrens, Behrens, Bergmann, Moser, Rauert, Stichler, Ambach, Eisner and PesslBehrens and others, 1971). There the minima in tritium contents in midsummer are explained by maximum shares of melt water from glacier ice that.is practically free of tritium. The reduction in tritium content of the discharge during spring is due to the low tritium content in the melt water from winter snow. Λ similar decrease in tritium content at the onset of winter snow melting has been found in the run-off of the Dischma basin (Switzerland) by Reference Martinec, Martinec, Siegenthaler, Oeschger and TongiorgiMartinec and others (1974) where it is limited, however, to the period of snow melt. There, however, it never reaches the minimum in tritium contents observed in the glacier streams of Rofental, because the Dischma basin is hardly glaciated—in contrast to the catchment area of Rofenache.

The curves of variation for the tritium contents of run-off from Hintereisferner and Rofenache are similar. However, the summer values in the Hintereisferner run-off are lower than in Rofenache ( Fig.10). In accordance with the daily variations in tritium content given by Reference Behrens, Behrens, Bergmann, Moser, Rauert, Stichler, Ambach, Eisner and PesslBehrens and others (1971), this shows that Hintereisbach during the ablation period has a greater proportion of melt water than Rofenache.

In consequence of different ablation conditions which are reflected by the difference in tritium contents in the run-off, ice ablation in the summer 1974 began later than in 1973. This has already been observed in the time variation of the deuterium content in the Rofenache run-off (Table IV) and may furthermore be confirmed by comparing the minima of tritium contents of Figure 10 which correspond to highest proportion of ice-melt water. Figure 10 also contains the tritium concentrations in the precipitation at Vent. The values are plotted as the weighted monthly means. Significant seasonal fluctuations are shown as well as the high values of spring 1974. The increase of tritium contents in spring 1974, however, is in agreement with the tritium increase observed in precipitation in other parts of Austria in May and June 1974 which were also higher than the year before (Reference Bauer, Bauer von, Rajner and RankBauer and others, 1975). Figure 10 furthermore shows the monthly means of the Rofenache discharge (Vent) illustrating the relation between high discharge due to strong ablation and low tritium concentrations.

Fig.11.

Decrease in tritium content in the winter run-off of Kesselwandferner (KWB) •. Hintereisferner [HEB) X, and Rofenache at Vent (RA) ○, and decrease in precipitation at Hohenpeissenberg (Bavaria) — — —, Petzenkirchen

(Austria) —, Wien —, and Vent (Austria) vvv. Curve drawn by estimation. (IAEA, 1971, 1973) Gratitude is expressed for the private information on measured data by the Isotope Hydrology Section of the IAEA, Wien.

Maximum tritium contents are always observed in the winter discharge. Figure r 1 gives the decrease in these maximum tritium contents for the years of 1968-74 (Fig. 10 and Reference Behrens, Behrens, Bergmann, Moser, Rauert, Stichler, Ambach, Eisner and PesslBehrens and others, 1971), as well as the annual means of tritium concentrations in the precipitations of various stations. All precipitation values are below the tritium contents in the respective winter run-offs ( Fig.10), if the annual mean values of the tritium content in the precipitation are taken as an approximate measure of the tritium input concentrations in the ground water system of the catchment area. It may be concluded that the winter discharge is being fed by water of precipitations of former years, containing more tritium. Reference Martinec, Martinec, Siegenthaler, Oeschger and TongiorgiMartinec and others (1974) have conducted model calculations for the Dischma basin, on the basis of which the mean residence time of the ground-water share in the discharge was estimated to be approximately four to five years. The models assumed for calculating the age distribution were the "exponential model" and the "dispersion model" with a ratio of 2/3 of winter recharge and 1/3 of summer recharge. The differences found between the two models were small.

A comparison with the results measured in the catchment area of Rofenache suggests that the residence times for the water of base-flow in the winter are similar. This, however, does not explain whether the base-flow originates mainly from melt water of long intraglacial storage or From the ground-water reserve of the soil.

It may thus be concluded that new information can be obtained on the proportions of melt water and spring water in the total discharge and on the residence time of the base-flow in the ground-water system of an Alpine glacier by measuring the contents of deuterium and tritium on samples from a glaciated catchment area.

3.1.Introduction

The pattern of the annual net accumulation in the accumulation area of Alpine glaciers have so far been determined by measuring vertical profiles of the gross beta activity only for periods of heavy atmospheric fall-out (Reference EisnerEisner, 1971). Because of the much lower radioactivity measured in air and precipitation samples during past years, it was doubtful if these methods were still applicable, especially as the role of natural radionuclides in the formation of activity horizons is still largely unknown. The present examination is intended to show whether the gross beta activity also yields characteristic vertical profiles in the accumulation area of Kesselwandferner during periods with comparatively low atmospheric fall-out (1966-73), and above all whether the summer melt horizons are clearly marked by activity peaks.

3.2.Results

In the accumulation area of Kesselwandferner, two drillings (I, II) down to about 12 m depth have been made with a SIPRE drill that had been improved by Reference EisnerEisner (1971). The drill core was cut into samples about 5 to 10 cm long, and the gross beta activity of the dry residue after evaporating the samples was measured with a low-level counter (background about 2 counts per minute). The sample preparation has been described in detail by Url (unpublished) and Elsässer (unpublished). The annual net accumulations from 1966 to 1973 were determined by means of the vertical profiles of the measured gross beta activity given in Figure 12. Good agreement was observed with results obtained independently from stake readings and determinations of water equivalents (Elsässer, unpublished).

While the firn activities of the summer horizons 1961-64 varied between 85 and 546 pCi/kg (Reference EisnerEisner, 1971 )—they were caused by heavy atmospheric fall-out—the activity values of the summer horizons of 1966-73, though well above the limit of identification, were no more than 6-69 pCi/kg.

Between the respective annual horizons there occur low gross beta activities with values smaller than 5 pCi/kg, as has been observed also by Reference EisnerEisner (1971). The decrease in horizon activities of the period of 1966 to 1973 as compared to that of 1961 to 1964 by approximately a factor of 10 is in good quantitative agreement with the decreasing gross beta activity of precipitation samples during this period ( Fig.13).

The activity peaks of the period 1961 to 1964 are around 3 000 pCi/1; those of the period of 1966 to 1973 are around 285 pCi/1 at a maximum. The maximum values of the gross beta activity of air samples are lower in the period 1966 to 1973 than between 1961 and 1964 (when they were 20 times higher).

Fig.12.

Vertical profile of the gross beta activity in the accumulation area of Kesselwandferner. I: drilling I. 3 225 m a.s.t., July 1973; II: drilling II. 3 167 m a.s.t., July 1973; activity measurements: October 1973 to January 1974. SH = summer horizon.

Profile a: Specific beta activity A_s (pCi/kg) of the firn sample; values < 1 pCi/kg have not been plotted.

Profile b: Specific beta activity A_s’ of the dry residue; values < 0.1 and 0.2 pCi/mg, respectively, have not been plotted.

Profile c: Specific dry residue g' (mg/kg) of the firn sample.

The value of the gross beta activity of a firn sample (units pCi/kg) may be given as the product of the following factors: A_β’ (units pCi/mg) and g’ (units mg/kg), with A_β' being the value of the specific gross beta activity related to the specific dry residue, and g' being the specific dry residue related to the mass of the firn sample. The depth profiles of A_β’ and g' are plotted in Figure 12. In many cases the values of A_β’ and g’ have a relative maximum in the summer horizons. This demonstrates that the peak values of the specific gross beta activity of the firn samples are accompanied by high values of A_β’ and g'. Horizon analyses based on vertical profiles of g' alone are not clear.

These results confirm that the mechanism described by the model of infiltration and adsorption of radionuclides (Reference Ambach, Ambach, Eisner and PrantlAmbach and others, 1968; Reference Prantl, Prantl, Ambach and EisnerPrantl and others, 1974) yields characteristic vertical profiles of gross beta activity in the accumulation area of an Alpine temperate glacier even during periods of low atmospheric fall-out. According to this model, summer ablation horizons are characterized by concentrated beta-active deposits that are bound to the horizons by adsorption. The percolating melt water does not wash-out this activity profile, but intensifies it secondarily, as the ablation horizon acts as an adsorption filter for the percolating melt water.

Fig.13.

Variation in gross beta activity for the years of 1958 to 1973.

(a) Precipitation samples A_βNS (pC/1);

(b) air sample A_βL, (pCi/m²).

Station: Wien (Hohe Warte), Innsbruck (Hygienisches Institut der Universität Innsbruck), and Garmisch (top of Berg Wank). (The respective institutions are thanked for making data available.)

Control measurements of the activity values in horizons yielded an "apparent half-life" of about two years, in agreement with former measurements by Url (unpublished). This relatively short "apparent half-life" of two years supports the assumption that the activity horizons are partly renewed by adsorption of short-lived nuclides, displaced from the snow surface by melt-water percolation.

In addition, the vertical distribution of tritium concentrations in a drill core from the neighboring drilling IV was studied. The decrease in tritium content upwards from a depth of 18 m was found to be in agreement with the gradual decrease in tritium concentrations in the precipitation of the past few years ( Fig.14). Relating the maximum tritium concentration of the profile with the accumulation in 1963 with its maximum tritium content in the precipitation, we obtain a mean annual net accumulation of 1.8 m of snow for the subsequent decade. This is in good agreement with horizon analyses from gross-beta-activity measurements in the drillings I and II covering the period of 1967-73, and also with former examinations of tritium profiles covering the period of 1954 63 made by Reference Ambach, Ambach, Eisner and SauzayAmbach and others (1969) in the vicinity of drilling IV.

Fig.14.

Vertical profile of the tritium content in core IV (Kesselwendferner, 3 227 m a.s.l., July 1973). The measured results refer to the date of sampling. The twofold standard deviations of the tritium concentrations are 3 to 7°₀.

Consequently it was found that measurements of tritium content in firn layers yield a reference horizon characterized by an especially high tritium concentration in the vertical profile. This may be attributed to the net accumulation of 1962-63. Adequate examination of the vertical distribution of gross beta activity in firn is a suitable means of analysing the net accumulation on Alpine glaciers, despite the low atmospheric Tall-out of the past decade.