Field Work

The SPIC, about 350 km long and 30–40 km wide, is situated between 48 °20′ and 51 °30′;s and 73 ° and 74 ° W.

The drilling site (50 °38′S, 73 °15′W, 2680 m a.s.l.) was located on a 100 km² gently sloping plateau, which is the accumulation area for several large glaciers Fig. 1. The sampling equipment, in particular the hand auger, and the operators were transported by helicopter from the edge of one of these glaciers (Perito Moreno). The firn core, placed immediately in an insulated box after drilling, was rapidly transferred to a freezer installed in a tourist bungalow located in the vicinity of the glacier. The temperature was measured at the bottom of the borehole 48 h after recovery of the firn core with the aid of a calibrated thermistor.

The firn core was cut into 45 sections at the bungalow. After density measurements, the core sections were sub-sampled for further isotope determinations. For chemical studies, the external part of each sample was removed using pre-cleaned tools by operators wearing clean-room clothes and masks. The firn samples were then transferred into sealed polyethylene bags and kept frozen until their analysis in Grenoble.

Laboratory Work

The samples were analyzed in the laboratory in clean-air conditions, according to the procedure of Reference Legrand, Delmas, Jones and Orville-ThomasLegrand and Delmas (1987). Major ions were determined by ion chromatography (Dionex 2010). The estimated precision was 10%. The stable-isotope content(δD%) was measured by mass spectrometry on the sub-samples collected in the field at Centre d’Etudes Nucléaires de Saclay, France.

Temperature

The temperature measured at the bottom of the borehole (13.17 m) was exactly 0 °C, indicating a temperate glacier. The mean annual temperature of the area, even at lower altitudes, is very poorly documented. We estimated the mean annual temperature at the drilling site tentatively using data collected at the meteorological stations of Lago Argentino (50 °20′S, 72 °18′W, 200 m a.s.l.), about 80km to the northeast, and Torres del Paine (51 °10′S, 72 °18′W, 125 m a.s.l.), about 60km to the south-southeast. The mean annual temperatures there were 7.3 °C (Servicio Meteorológico Nacional de la República Argentina) and 7 °C (personal comunication from W. C. Keene), respectively. The altitudinal temperature lapse rate used in the calculation is 0.53 °C/100m. This value, which is very close to the net adiabatic lapse rate, was obtained by Reference Inoue, Kondo, Fujiyoshi, Yamada, Fukami and NakajimaInoue and others (1987) for the northern Patagonia ice cap. The temperature calculated in this way is approximately −6 °C, a figure relatively low in comparison with the Quelccaya Ice Cap (–3 °C), which prevents excessive percolation.

Density

The physical appearance of the shallow snow layers is typical of a temperate glacier, with coarse grains and numerous ice layers 0.5–30 mm thick. Consequently, the density (d) profile is irregular, which is also characteristic of temperate glaciers. It can be represented by the linear regression (R² =0.78) of the 37 levels measured: d = 20z + 406 (d in kg m⁻³ and z in m). The mean value (606 kg m⁻³) at 10 m depth and the transition depth of firn to ice (20–25 m, by extrapolation) are comparable to corresponding values obtained on the Quelccaya Ice Cap (64Q k gm⁻³; Reference ThompsonThompson, 1980) and on Vernagtferner (640 kgm⁻³ and 20–25 m; Reference Oerter, Reinwarth and RufliOerter and others, 1983). Similar values were also obtained on the northern Patagonia ice cap (Reference YamadaYamada, 1987), despite the different densification process due to the large amount of water present in the snow.

Isotope Measurements, Dating and Snow-Accumulation Rate

The isotopic composition (O and Η atoms) of polar snow depends on atmospheric temperature (Reference DansgaardDansgaard, 1964). Temperature changes, in particular seasonal cycles, are therefore naturally recorded in polar ice caps. These seasonal variations are commonly used for dating firn and ice layers (Reference Hammer, Oeschger and LangwayHammer, 1989). On the other hand, for glaciers located at mid or tropical latitudes, meltwater percolation tends to destroy seasonal patterns and to homogenize the isotopic composition. For temperate glaciers, the effect is particularly well marked, and only in special cases (conjunction of particular meteorological and physical conditions) do the isotopic profiles still contain information usable for climatic and dating purposes (Reference Stichler, Baker, Oerter and TrimbornStichler and others, 1983; Reference Thompson, Grootes, Pourchet and HastenrathThompson and others, 1984). At our site, the relatively low estimated mean annual temperature (−6 °C) and local meteorological conditions (high precipitation rate, prevailing westerly Pacific winds and frequent cloudiness which reduced summer melting) are favourable factors for the preservation of the initial stratification of the snow layers. The isotopic profile Fig. 2 exhibits fluctuations which can reasonably be attributed to seasonal variations. The core was dated on the basis of the visual glaciological stratigraphy reported in Figure 3, combined with the interpretation of this isotope profile. The winters of 1982, 1984, 1985 and 1986 (date of field work) and the summers of 1980–81, 1983–84, 1984–85 and 1985–86 are clearly identified.

Fig. 2. Seasonal variations of the deuterium content compared with the snow stratigraphy. Water-equivalent depth (7.07 m at the bottom) is calculated using the mean density profile. Black segments represent ice layers (0.5–30 mm thick). Open circles represent ice lenses.

Fig. 3. Concentration profiles of the various ions determined in the firn core and Cl⁻/Na⁺ ratio as a function of depth. The time-scale is given by the isotope profile (upper curve).

A mean value of 1.2 m water equivalent (w.e.) is deduced for the annual accumulation rate. This is only one-third of what can be expected from data obtained at nearby temporary stations (Agua y Energía, 1978) using their precipitation versus longitude gradient. Such a difference, also observed on the northern Patagonia ice cap (Reference Fujiyoshi, Kondo, Inoue and YamadaFujiyoshi and others, 1987; Reference YamadaYamada, 1987), could be caused by the strong and frequent winds prevailing in the area (which blow away snow layers) and/or by some surface melting. This second explanation is less likely because of the absence of significant percolation patterns, as mentioned earlier. Finally, we cannot entirely rule out an erroneous interpretation of the annual signals, which could lead to a smaller value for the number of years encompassed by this core due, for instance, to the occurrence of two isotope peaks per year as is sometimes observed (for example, at Mont Blanc by Reference Jouzel, Legrand, Pinglot, Pourchet and ReynaudJouzel and others (1984)).

Chemical Measurements

In temperate glaciers, the depth profiles of chemical species are generally significantly disturbed by meltwater percolation. When a water table forms, most of the soluble impurities are washed out and seasonal variations may be replaced by other fluctuations linked with the up and down movement of the water level. No information is available on whether this phenomenon occurs in the deeper firn layers. In the upper firn layers, a memory of the initial seasonal variations can persist for several years, provided percolation is not too intense. This seems to be the case at the study site, according to visual observations in the field (the ice core was “dry” and the borehole free of water) and to the persistence of the seasonal isotopic patterns.

Chemical depth profiles are shown in Figure 3. Suphate and nitrate concentrations both exhibit a rapid decrease (by more than 50%) in the first 3 m (i.e. about 2 years). This part of the profile can be represented satisfactorily by exponential functions with r ²=0.68 and 0.66 for SO₄ ²⁻ and NO₃ ⁻, respectively. The ratio Cl⁻Na⁺ is 1.13 for the first year of accumulation, a value very close to the marine reference value (1.16). This observation is in agreement with the marine origin of the air masses in the area, as was also found at Torres del Paine (Table 1; Cl⁻Na⁺ = 1.17). However, this ratio decreases markedly as a function of depth Fig. 3, which indicates that Cl⁻ is preferentially eluted to Na ⁺. Below a depth of 3 m, nitrate values continue to decrease, but more slowly, whereas sulphate values remain relatively stable around 0.4μeq. l⁻¹. For Cl⁻¹ and Na⁺, the decrease is much less marked and high values are still observed after 4 or 5 years. The K⁺ and NH₄ ⁺ profiles appear to be independent of depth.

Table 1. Chemical concentrations (C, μeq. 1⁻¹) and deposition fluxes (ϕ, μM m⁻²a^δ1) in snow at the study site (southern Patagonia ice cap). The values are mean values obtained from the six shallowest samples (about 1 year of precipitation, see text). Precipitation chemistry data from Torres del Paine precipitation station (51 ° 10′ S, 72 ° 58′W, 125 m a.s.l.; Reference Likens, Keene, Miller and GallowayLikens and others, 1987) and from JamesRoss Island, Antarctic Peninsula (mean values over 130 years; Aristarain and others, unpublished), are also reported for comparison. Corresponding deposition fluxes (ϕ) are calculated using the water-deposition rates R_w (m of water a⁻)

We can therefore conclude that the following elution sequence is obtained:

We have therefore decided to consider only the last year of precipitation (six samples, from the winter of 1985 to the winter of 1986) as being representative of the actual levels of chemical impurities in the local precipitation, bearing in mind, however, that these values are possibly only lower bounds. These data are compared to the measurements at Torres del Paine (Reference Likens, Keene, Miller and GallowayLikens and others, 1987), which is the closest station with existing precipitation chemical data (Table 1). All concentrations, except for NH₄ ⁺, are lower at our southern Patagonia site than at the Torres del Paine site (as shown by the SPIC/ PAINE ratios for Na⁺: 0.23, C⁻: 0.22, nssSO₄ ²⁻: 0.31, NO₃ ⁻: 0.64 and K⁺: 0.46), in agreement with the large elevation difference between the two sites.

Nevertheless, potassium concentrations are relatively high on the southern Patagonia ice cap, in comparison with what might be expected from the marine source. Note that the K ⁺/Na⁺ ratio (0.15) reported in Table 1 is significantly higher than both the marine reference ratio (0.023) and the ratio reported for Torres del Paine precipitation (0.07). Excess potassium could be linked to either a local crustal source or a contribution by vegetation. In the absence of calcium data, it is difficult to favour one of these hypotheses, even if the second appears to be less likely due to the paucity of vegetation in these areas.

A further comparison with the concentrations obtained on James Ross Island, Antarctic Peninsula (elevation 1640 m), reveals that gas-derived compounds (nssSO₄ ²⁻ and NO₃ ⁻) have very similar concentrations on both ice caps, which could therefore be considered as representing background reference values for the mid to high latitudes in the southern Pacific Ocean.

These latitudes are very remote from large populated, industrial or agricultural centres. Anthropogenic sulphur and nitrogen compound levels are very low there as the atmosphere is constantly cleaned by heavy rains. It can therefore be assumed that the concentrations of gas-derived aerosol or gases (excess SO₄ ²⁻ and NO₃ ⁻) are representative of the natural levels of freshly formed sulphate aerosol and gaseous HNO₃, or from aged compounds transported in the free troposphere.

Our results at this location cover a very limited time period and it is difficult to evaluate what happens deeper in the glacier. We can only refer to the two temperate deep ice cores recovered from the Quelccaya Ice Cap (about 1.5 × 10³ year; Reference Thompson, Mosley-Thompson, Dansgaard and GrootesThompson and others, 1986, Reference Thompson, Davis, Mosley-Thompson and Liu1988), where a useful conductometric profile was obtained, and to northern Spitsbergen, where pH and conductivity measurements cover possibly 6000 years (Reference FujiiFujii and others, 1990). Reference Punning, Martma, Tyugu, Vaykmyae, Pourchet and PinglotPunning and others (1986) claimed they observed seasonal Cl⁻ variations at considerable depths in Nordaustlandet, Svalbard.