Introduction

Current emphasis upon the comprehensive investigation of the global environmental system (National Research Council, 1986, p. 1–6, 1988) has drawn attention to ice sheets and ice caps which continuously record and preserve the physical and chemical character of the atmosphere. The extraction of an environmental history from an ice core requires evaluation of both the temporal quality and spatial variability of the record which limits its utility as an environmental proxy. The gases trapped in ice bubbles at Siple Station have provided a unique, high-resolution record of atmospheric chemistry (Reference Stauffer and OeschgerStauffer and Oeschger, 1985; Reference Friedli, Lotscher, Oeschger, Siegenthalcr and StaufferFriedli and others, 1986). Here we explore the potential of the δ¹⁸0, particulate, and chemical records anticipated from a 302 m core for reconstruction of paleoenvironmental conditions in the high southern latitudes.

In support of deeper cores (302 and 132 m) drilled at Siple Station, Antarctica (75°55′S, 84°15′W, 1054 m a.s.l.; Fig. 1), during the 1985–86 austral summer (Reference Mosley-Thompson, Mountain and Paskie–vitchMoslcy-Thompson and others, 1986), eight additional shallow cores (20 m) were collected and samples were taken from three pits. The 20 m core records encompass 20 years (AD 1966–85) and in combination with pit studies represent a sampling area of several km². These have been used to examine the potential for accurate dating, to obtain basic glaciological information such as annual accumulation rate and density variations with depth, to examine the spatial reproducibility of the preserved records, and to assess their relevance to larger-scale processes.

Fig. 1. Antarctic sites for results cited in the text and in Table 1.

Soluble impurities in Antarctic snow and ice provide unique information about both present and past atmospheric chemical composition. Siple Station, located near the base of the Antarctic Peninsula (Fig. 1), offers the opportunity to study precipitation chemistry at a site intermediate between the coastal areas, where sea-salt aerosol has a strong influence and the interior where secondary aerosol tends to be dominant. For the purposes of this paper, the Antarctic seasons are loosely defined as: summer, December-February; winter, March-September; and spring, October-November.

Sample Acquisition, Preparation And Analyses

Drilling and pit sampling were conducted 2 km upwind of the station to reduce the potential of contamination. All cores and pit samples were stored below −20°C until just prior to laboratory analysis. Samples were initially prepared in a cold working room (−15°C) where a band saw was used to cut the samples directly from the core. A minimum of 20 mm of material was removed from all sides to obtain fresh samples of the desired size which were placed in pre-clcaned containers. With the exception of the δ¹⁸O samples, further cleaning, melting and analysis were conducted in a Class-100 clean-room laboratory.

Table 1. Chloride, nitrate and sulfate in Antarctic snow

∼ Estimated from diagrams.

– Information not available.

Millipore Milli-Q ultra-pure, deionized, filtered water was used for cleaning of all samples and containers and for preparing eluants and standards. The concentration of insoluble microparticlcs with diameters (MPC) were measured by a Model TA II Coulter counter, using a procedure described elsewhere (Reference ThompsonThompson, 1977). The electrical conductivity (EC) of liquid samples was measured using a Beekman RC-20 conductivity bridge. The δ¹⁸Ο measurements were made with a stable-isotope mass spectrometer at the Quaternary Isotope Laboratory of the University of Washington.

The anion concentrations were determined with a Dionex Model 2010i ion Chromatograph equipped with an AS4A anion separator column and a micro-membrane suppressor column. Carbonate/bicarbonate (0.0012/0.00038 mol 1⁻¹) eluant was used, along with 0.1 mol 1¹ H₂SO₄ as regenerant for the suppressor. Analytical precision and sensitivity were significantly improved over the method previously reported by Reference Legrand, DeAngelis and DelmasLegrand and others (1984) which has been recently upgraded by Reference Saigne, Kirchner and LegrandSaigne and others (1987). The use of a relatively large injection loop (0.64 ml) eliminated the need for a concentrator column (Reference ArbogastArbogast, 1987), while preserving the desired detection limits (c. ∼ 1 ppb for Cl, NO₃, and SO₄ ²). Working standards were prepared daily from stock solutions and procedural blanks were included in each analytical session for every step in sample handling, beginning with the cutting by band saw. Only minor amounts ( < 5 ppb) of Cl were observed in a few cases. The time required for each analysis (injection) is approximately 10 min. The ionic concentrations are comparable to previously published values (Table 1), suggesting that the contamination control procedures employed are effective.

Shallow-Core Results: (ad 1966–85)

Oxygen-isotope ratios (δ¹⁸Ο)

Figure 2 illustrates δ¹⁸Ο for three 20 m cores (cores 2, 6 and 8) and the upper 18 m of core A which was drilled in a 2 m trench. The depth in firn was converted to water-equivalent depth using the depth-density relationship derived from density measurements in pits and on cores. Figure 2 clearly demonstrates that δ¹⁸O exhibits a consistent seasonal signal as previously demonstrated by Swiss analyses of a 1983 core. Their work on a single core did not allow investigation of the spatial reproducibility of the δ¹⁸Ο records. Near the surface, sub-annual events (e.g. 1983–82 and 1982–81) are preserved from one site to another; however, below 3 m, these events are smoothed. Signal reproducibility is evident.

Fig. 2. Oxygen-isotope (δ¹⁸O) ratios fir three 20 cm cores (2, 6 and 8) and the upper 18m of core A illustrate the spatial reproducibility of the record. The firn depths were converted to water-equivalent depths using a depth-density relationship derived empirically from pit- and core-density data.

Table 2. δ¹⁸O results from four 20 m cores (AD 1966–85). Pearson correlation coefficients and significance levels

NS: Not significant at any acceptable level (<90%).

(σ): Significance level.

Number of observations: 20 for cores 2, 6 and 8, and 18 for core A.

A statistical examination (Table 2) reveals significant correlations among all four cores for winter averages and among cores 2, 6 and 8 for both annual and summer averages. The seasonal averages consist of all values in a given year which are above or below the 20 year mean for the respective core. The lower correlations for summer probably reflect the increased control of topography upon the surface-energy balance during periods of little or zero accumulation. Core A is correlated least with the other cores and there are no obvious differences in handling or analysis. However, core A contains only 18 years which means there are two less degrees of freedom which lowers the significance level. Excellent correlations among cores 2, 6 and 8 for both annual and intra-annual periods suggest that δ¹⁸O trends in deeper cores should be representative of the Siple Station area.

Insoluble microparticle concentrations (MPC)

Figure 3 presents the MPC, δ¹⁸Ο and EC profiles for two 20 m cores (cores 7 and 8). The MPC and EC profiles have been smoothed with a three-sample unweighted running mean. Particulate concentrations are the lowest measured in Antarctica (Reference Thompson and Mosley–ThompsonThompson and Mosley-Thompson, 1982) which necessitated using a sub-coring device to remove samples from the interior of the core. Although particulate concentrations vary seasonally, the low concentrations often approach background levels. Smoothing enhances the seasonal signal (Fig. 3), but insoluble particulates do not provide a reliable means for dating deeper cores. The very low concentrations attest to the lack of a significant contribution from local sources. In fact, with such low background concentrations, the Siple Station cores should provide an excellent record of major dust events reaching the high southern latitudes.

Fig. 3. Microparticle concentrations and electrical conductivity of liquid samples in core 7 are illustrated along with their respective three-sample unweighted running mean. The time-scale based on the core 8 δ¹⁸O record is illustrated.

Anionic chemistry

Core 6 was devoted to δ¹⁸O and anion analyses. 284 samples of approximately 70 mm length were cut from the 20 m core providing a range of 1–22 samples per year. The flux (mass/area) of each anion was calculated by multiplying the concentration by the sample length (in water equivalent). The annual flux for each anion is the sum of the fluxes for each year. Negative values of excess sulfate (discussed below) were excluded from annual flux calculations.

Concentrations of major soluble chemical species (Table 1) have been measured by other researchers in snow and ice samples from various areas in Antarctica (Fig. 1). Our results are in excellent agreement with previously reported analyses of Siple Station samples (Reference HerronHerron, 1982).

Chloride

Reference Legrand and DelmasLegrand and Delmas (1984) demonstrated that chloride in polar snow results mainly from the deposition of sea-salt aerosol (as NaCl), particularly in coastal areas. On Dolleman Island in the Antarctic Peninsula, sea-salt chloride comprises ≈95% of total chloride (Reference Mulvaney and PeelMulvancy and Peel, 1988). Chloride levels at Siple Station (Table 1) fall between the high levels at coastal sites (e.g. James Ross Island and Dolleman Island) and the low levels at continental sites (e.g. South Pole). Legrand and Delmas estimated sea-salt chloride to be 50–60% of total chloride at the South Pole. Consequently, sea-salt chloride at Siple Station is probably a dominant part of total chloride, between 60 and 95%.

Figure 4 illustrates that chloride exhibits an annual cycle with highest concentrations generally associated with winter precipitation. However, during winter and perhaps early spring multiple-concentration maxima are common. The multiple-concentration peaks are evident in the snow-pit samples (not illustrated). Reference Mulvaney and PeelMulvaney and Peel (1988) reported a clear annual peak in chloride concentration in snow on Dolleman Island, corresponding to the late summer/autumn period, which they attributed to minimum sea-ice extent in the Weddell Sea. At another coastal site close to the Weddell Sea, Reference Wagenbach, Gorlach, Moser and MünnichWagenbach and others (1988) reported a concentration maximum of sea-salt aerosol in autumn. Located further from the Weddell Sea, Siple Station is unlikely to receive the abundance of summer/autumn sea-salt aerosol that produces the annual chloride peak on Dolleman Island. The much lower chloride concentrations at Siple Station (Table 1) supported this. The different season for maximum chloride concentrations also suggests that seasonal variations in sea-salt aerosol at Siple Station are not closely associated with sea-ice conditions in the Weddell Sea region.

Sulfate

It is well established that sulfate concentration in Antarctic snow varies seasonally. Annual summer maxima and winter minima have been observed on the Antarctic Peninsula (Reference Aristarain, Delmas and BriatAristarain and others, 1982; Reference Mulvaney and PeelMulvaney and Peel, 1988), in East Antarctica (Reference Legrand and DelmasLegrand and Delmas, 1985) and at the South Pole (Reference Legrand and DelmasLegrand and Delmas, 1984). Measuring the sulfate concentration in ground-level aerosols, Reference Wagenbach, Gorlach, Moser and MünnichWagenbach and others (1988) found a prominent seasonal cycle similar to that in snow. The unsmoothed sulfate profile for the 20 m firn core exhibits fairly regular annual cycles (Fig. 4). Of the three anions (Cl_-, SO₄ ^2- and

), sulfate exhibits the best annual signal and appears to be a useful dating tool in this area.

Fig. 4. Concentrations (μeq 1^-1) of chloride, sulfate, excess sulfate, and nitrate from core 6 are illustrated along with δ¹⁸O used to date the core. Excess sulfate is estimated according to Equation (1). Off-scale concentrations are provided.

Fig. 5. Annual fluxes of chloride, sulfate, excess sulfate (excluding negative values), and nitrate, 1966–85, are illustrated along with annual net accumulation from core 6.

Excess sulfate (sulfate contributions not from sea salt), has been calculated according to Equation (1) where if (0.103) is the ratio of sulfate/chloride (μequivalent 1⁻¹) in bulk sea water. It would be more appropriate to use sodium concentrations instead of chloride because non-sea-salt chloride may be present. However, sodium measurements are unavailable and thus Equation (1) is used for calculating excess sulfate. The error introduced by using total chloride in Equation (1) is estimated to be no more than 10% of excess sulfate.

(1)

Since chloride and total sulfate annual cycles are out of phase by ˜6 months, the excess sulfate profile, which is essentially differentiation of sulfate and chloride, exhibits a more prominent annual signal than either chloride or sulfate. For example, Figure 4 clearly illustrates that the slightly ambiguous sulfate maxima in 1973 and 1974 are much more prominent in the excess sulfate profile. This profile also reveals that background (winter) excess sulfate concentration is generally close to zero. In 13 of the 284 samples, the calculated excess sulfate is substantially negative.

The annual sulfate-flux profile (Fig. 5) contains two peaks. The less prominent one in 1983 could reflect elevated annual accumulation. In contrast, the flux for 1976 is 3.5 μg cm⁻², 75% higher than the 20 year annual average of 2.0 μg cm⁻². The sulfate flux for the previous year (1975) is also slightly elevated. A sudden increase in sulfate often indicates the presence of volcanic sulfate. Reference Aristarain, Delmas and BriatAristarain and others (1982) found two large acidity peaks in the James Ross Island core which were tentatively attributed to the February 1975 eruption of Mount Ngauruhoc ( 37° S, 174°E) and to the 1963 eruption of Mount Agung (08.3° S, 174°E). The large sulfate flux in 1976 at Siple Station may also reflect the Mount Ngauruhoe eruption. The Mount Agung eruption is not contained in the sulfate record presented here as the shallow cores do not extend to 1963–64.

This and previous work by others (e.g. Reference Delmas, Legrand, Aristarain and ZanoliniDelmas and others, 1985) suggest that sulfate deposited from a small or moderate volcanic eruption is primarily restricted to a single year, and in many cases, to the summer maximum. Notice that the winter concentration minima before and after the 1976 sulfate peak (Fig. 4) are virtually unchanged. The extremely high concentrations or flux of sulfate are restricted to a very narrow depth interval (one or two samples, or ≈10cm in w.e., corresponding to midsummer (December-January). The time lapse between the eruption (February 1975) and the maximum deposition (∼ December 1976) is much longer than required for the oxidation of the volcanic sulfur species (SO₂) to sulfate in the presence of light (Reference McKeen, Liu and KiangMcKeen and others, 1984). The presence of slightly elevated sulfate concentrations in 1975 summer snow suggests that at least part of the Mount Ngauruhoe volcanic gases reached this latitude, where sunlight is available only in summer. This implies that volcanic sulfur, although present in the atmosphere at this latitude, was not being removed as sulfate during the winter months. Indeed, the Siple Station data indicate virtually no sulfate deposition, except that from sea salt, in the austral night. Therefore, it appears that the rate of sulfate deposition reflects the availability of sunlight.

The major volcanic sulfur species (SO₂) and organo-sulfur species from marine biogenic activity, which are the precursors of excess sulfate (Reference Legrand and DelmasLegrand and Delmas, 1984), must be chemically transformed (oxidized) before surface deposition. Thus, in the overall process of marine and volcanic production, transportation, chemical transformation, and deposition of atmospheric sulfur in high southern latitudes, the rate-controlling factor appears to be photochemical oxidation. The subsequent deposition of sulfate is believed to be rapid because of efficient scavenging by precipitation of sulfate (as sulfuric acid) which serves as excellent condensation nuclei.

Nitrate

Nitrate concentrations vary less than those of chloride and sulfate. For the 284 samples, the ratio of standard deviation to the average is 0.49 for nitrate, compared to 1.4 for chloride and 0.71 for sulfate. Reference Aristarain, Delmas and BriatAristarain and others (1982) reported similar observations of nitrate concentrations with a relatively constant background level perturbed only by sporadic increases of unknown nature. The absence of extremely high concentrations, which are common for sulfate, suggests the absence of explosive sources such as volcanic eruptions. Antarctic nitrate concentrations are compared in Table 1. The average concentration at Siple Station (Reference HerronHerron, 1982, this work) compares well with those from three other Antarctic Peninsula sites (Gomez Nuntak, Dolleman Island and James Ross Island). Thus, nitrate concentrations do not vary greatly in this part of the continent.

Reference HerronHerron (1982) suggested the possibility of a constant nitrate flux over the Antarctic continent, in response to or resulting from an inversely proportional relationship between concentration and snow-accumulation rate. Data in Table 1 do not support this. The fluxes for eastern Antarctic sites (e.g. South Pole) and the Ross Ice Shelf arc smaller than those for the Antarctic Peninsula sites.

An annual cycle in nitrate concentration similar to that of sulfate has been reported for Antarctica (Reference HerronHerron, 1982; Reference Legrand and DelmasLegrand and Delmas, 1984; Reference LairdZeller and others, 1986). In the 20 years covered by this record, annual nitrate cycles are recognizable in some instances (e.g. 1974–82) and are ambiguous in others. In years with recognizable cycles, most nitrate peak concentrations occur just before the summer δ¹⁸O maxima, unlike the sulfate maximum in mid-summer. Actual measurements of coastal aerosols (Reference Wagenbach, Gorlach, Moser and MünnichWagenbach and others, 1988) show that atmospheric nitrate concentration peaks in spring. At the South Pole, Reference Legrand and DelmasLegrand and Delmas (1984) found maximum annual nitrate concentrations shortly after summer. This discrepancy suggests that nitrate seasonality may not be consistent at all sites. The frequent high concentrations in spring reported here indicate that nitrate deposition may be related to springtime atmospheric chemistry and/or vertical movement of polar air masses.

Reference LairdZeller and others (1986) cited large solar flares as potential sources of unusually high nitrate fluxes for 1972 and 1984 at a site on the Ross Ice Shelf. Neither the nitrate concentrations nor the flux profile from Siple Station contains such unusual peaks. Only the 1983 nitrate flux (2.76 μg cm⁻²) is substantially larger than the 20 year average (1.52 μg cm⁻²). This appears to result from the combination of unusually high annual accumulation (0.70 m) with the highest single nitrate concentration.

Net Accumulation

The reconstruction of a representative accumulation history from longer cores requires that spatial variability in net accumulation (A _n) be low. Two independent data sets suggest strongly that A _n is nearly constant from site to site. Reference StaufferNeftel and others (1985) reported a distinct melt layer in the summer of 1976 at 7 m below the 1983 surface. This same melt feature was present in eight of the ten cores drilled in 1985 and its depth varied from 10.46 to 10.63 m below the December 1985 surface. The depth of the 1976 feature, coupled with the depth–density relationship, indicates a 10 year average annual accumulation of 0.56 m (w.e.).

Using the δ¹⁸O seasonal variations, annual layer thicknesses in water equivalent were reconstructed using the depth–density relationship. The 20 year averages of A _n are 0.56 m w.e. for cores 2, 6 and 8, and 0.57 m w.e. for core A. Results of a linear correlation of A _n among the cores (Table 3) and the spatially consistent depth of the 1976 melt layer illustrate that accumulation has not varied substantially from one site to another over the last 20 years.

Anion Fluxes

Since the mid to late 1970s, there has been an increasing awareness of changes in the concentrations of atmospheric trace gases. In the South Polar regions, the most notable observation is the progressive decrease of ozone and the resulting increase in the size of the Antarctic ozone “hole”. While debates continue over the exact causes of the ozone decline, it is generally accepted that ozone destruction is the result of complicated chemical reactions involving atmospheric species of chlorine and nitrogen (Reference Farman, Gardiner and ShanklinFarman and others, 1985).

Table 3. Pearson correlation coefficients and significance levels for an annual layer thickness in four shallow cores

(σ): Significance level.

Number of observations: 20 for cores 2, 6 and 8; 18 for core A.

The exact effects which might be observed at ground level in response to changes in the stratosphere are undetermined. However, as the anions measured in this work may have stratospheric pathways, it is interesting to examine trends in their fluxes over the last two decades. The annual fluxes of chloride and sulfate are quite variable (Fig. 5). The 5 year average annual fluxes for chloride, sulfate, excess sulfate and nitrate, and the deviations from their respective 20 year means are given in Table 4 along with the annual accumulation (w.e.). The fluctuations in net annual accumulation are insufficient to cause large variations in the fluxes.

As discussed earlier, sea-salt aerosol accounts for most chloride in snow at Siple Station. A change in chloride flux at this location probably reflects a perturbation of conditions at ground level or in the lower troposphere and, therefore, is probably unrelated to stratospheric chemistry. Sulfate flux shows no particular pattern and the large flux for 1976–80 reflects partially the probable volcanic input of 1975–76. There is no evidence suggesting a direct involvement of sulfur species in the destruction of stratospheric ozone.

Nitrate flux is lowest for 1971–75. A substantial increase (~7–8%) is shown for each of the next two 5 year periods. Reference HeathHeath (1988) reported that during this decade, 1976–85, the loss of ozone in the South Polar region was progressing at a somewhat similar rate. However, an attempt to link the increase of nitrate flux to the ozone loss would have to explain the even higher flux of 1966–70. Clearly, a longer record is needed to examine the natural variability of nitrate flux and a better understanding of nitrate sources is essential.

Surface Temperatures And The δ¹⁸Ο Record

Siple Station (1054m a.s.l.) is located in an area where the complex near-surface wind regime of the Antarctic Peninsula region (Reference Schwerdtfeger and AmaturoSchwerdtfeger and Amaturo, 1979) and that of the high inland plateau converge. Hence, Siple Station may occupy a sensitive climatic setting ideal for isolating longer-term large-scale environmental changes affecting the entire region.

Although δ¹⁸O reflects other environmental factors in addition to condensation temperature, this record is interpreted strictly on the basis of temperature (more negative — cooler; less negative — warmer). Annual δ¹⁸Ο averages were possible because of the excellent annual resolution and are compared with surface temperatures for 1957–85 reconstructed from continental stations and several surrounding island stations. The temperature data were obtained from the National Center for Atmospheric Research and were updated using Reference Jones and LimbertJones and Limbert (1987) and the Antarctic Journal of the United States.

With a few exceptions, extreme temperature departures in a single year or season at one station are not necessarily recorded at others. This is particularly true for coastal stations where mesoscale processes may reflect local topography. However, most multi-year trends in both the Faraday and the Amundsen-Scott records (Fig. 6) are reflected in the Siple Station record. Specifically, these are the gradual warming throughout the 1960s, the persistent warmth from 1970 to 1975, and the onset of cooling around 1975. Since 1980, temperatures in the Antarctic Peninsula and the δ¹⁸O record at Siple Station indicate strong warming while cooling has prevailed at the South Pole.

For a larger-scale perspective, two different analyses of surface temperatures (T _s) for high southern latitudes are compared with the Siple Station δ¹⁸Ο history (Fig. 7). Reference Hansen and LebedeffHansen and Lebedeff (1987) combined T _s (Fig. 7b) for stations from 64° to 90° S using a method which minimizes the effects of incomplete spatial and temporal coverage and estimates the area over which the temperature change calculated from a given station is meaningful. Reference Raper, Wigley, Mayes, Jones and SalingerRaper and others (1984) used monthly surface temperatures from 16 stations (65° to 90° S) to produce an areally weighted average for 5° latitude by 10° longitude grid cells. The spatial characteristics of the annual and seasonal variations were examined using principal-component analysis (Reference Raper, Wigley, Mayes, Jones and SalingerRaper and others, 1984, fig. 6). The time series of the first principal component (PC–1) of annual temperatures (Fig. 7c) explains 35.8% of the variance. The loadings are positive over all of Antarctica except the sector from 40°Ε to 30°W, where they are slightly negative. The loadings are strongly positive in the Antarctic Peninsula region, e.g. loadings at Faraday and Siple Station are 0.6 and 0.3, respectively. The trends in annual δ¹⁸Ο at Siple Station and T _s at Faraday (Fig. 6) are consistent with the positive loadings. Amundsen-Scott lies just to the positive side of the 0.0 contour, suggesting little trend in T _s which is evident in Figure 6. These analyses suggest that South Pole Station may lie near the convergence of two dominant climatic regimes and, thus, may not offer a dependable and/or consistent representation of either regime over longer time-scales. However, its location in a climatically sensitive area could make the South Pole an excellent site for examination of major large-scale atmospheric circulation changes.

Table 4. Average annual fluxes at Siple Station for the last two decades

Fig. 6. a. Mean annual temperatures (as departures from 1957–86 mean) for Faraday, Antarctica (Reference Jones and LimbertJones and Limbert, 1987); (b) Annual δ¹⁸O record (as departures from 1957–85 mean) from Siple Station, Antarctica; (c) Mean annual temperatures (as departures from 1957–85 mean) for Amundsen–Scott South Pole Station, Antarctica (Reference Jones and LimbertJones and Limbert, 1987). These illustrate that extreme annual events at one site may not be recorded elsewhere. However, the broad trends at both Faraday and Amundsen–Scott are also reflected in the Siple Station δ¹⁸O record.

The most prominent feature in all the records is the persistent warmth from 1970 to 1975 (Figs 6 and 7) noted by Reference Swanson and TrenberthSwanson and Trenberth (1981) and Reference LimbertLimbert (1984). Reference SchwerdtfegerSchwerdtfeger (1976) reported a “remarkable” and statistically significant change in the Antarctic Peninsula temperature field in 1970. The relationship between temperatures at the Argentine Islands (65.13°S) and Oreadas (60.7°S), in which the mean annual temperatures at the former were consistently lower for the previous 14 years (1957–70), reversed in 1970. An analysis of the sea-level pressure field (Reference SchwerdtfegerSchwerdtfeger, 1976) suggested an increase in the frequency and strength of winds from the northwest advecting warmer maritime air from the open water of the southeastern Pacific Ocean to the west and northwest side of the Antarctic Peninsula. The recent work by Reference Raper, Wigley, Mayes, Jones and SalingerRaper and others (1984) and Reference Hansen and LebedeffHansen and Lebedeff (1987) indicates that the change in the early 1970s affected an area larger than the western coast of the Antarctic Peninsula. The δ¹⁸O record from Siple Station documents this large-scale event.

Fig. 7. The Siple Station annual δ¹⁸O record (departures from 1957–85 mean) is compared with temperature trends (departures from 1957–87 mean) for the 64° to 90° S zone (Reference Hansen and LebedeffHansen and Lebedeff, 1987) and with the 65–90° S. annual temperature departure (from the 1957–82 mean) of the first principal component for areally weighted Antarctica temperature data (Reference Raper, Wigley, Mayes, Jones and SalingerRaper and others, 1984). The Siple Station record reflects the same broad trends, although differences exist from year to year. Most prominent are the warming trend in the 1960s and the persistent warmth from 1970 to 1975, followed by cooling later in the decade and warming in the 1980s.

The Siple Station δ¹⁸O record reflects the principal features of both large-scale temperature trends for 64° to 90° S (Fig. 6) and Faraday (with the exception of the extreme value in 1980). As noted earlier, an individual station or recording site experiences short-term, localized events which may not be spatially representative over long distances. However, the data presented in Figure 7 illustrate that the broad trends in the Siple Station δ¹⁸Ο record are consistent with the areally averaged Antarctic temperature trends from 1966 to 1985 and reflect even more strongly trends in the Antarctic Peninsula region.

The δ¹⁸O record from Siple Station can be compared with several other annually resolved δ¹⁸O and deuterium (δD) histories. A 130 year δD record is available from Dalinger Dome (core D-81) on James Ross Island near the tip of the Antarctic Peninsula (Reference Aristarain, Jouzel and PourchetAristarian and others, 1986). The 1970–75 warm event is recorded by δD in the same manner as the Siple Station δ¹⁸Ο record, that is, by an overall trend of enrichment and reduced winter depletion. The latter probably reflects the shorter duration of winter and increasing warmth of each season during this time (Reference LimbertLimbert, 1984). The James Ross Island record is the first and longest ice-core reconstruction for the Antarctic Peninsula region and corresponds fairly well with the Oreadas record extending back to AD 1903. When the longer record is available from Siple Station, these two records should reveal whether multi-year temperature trends near the tip and base of the Antarctic Peninsula are synchronous.

A similar comparison can be made with the δ¹⁸O histories from Dolleman Island (70°35.2′S, 60°55.5′W) and Gomez Nunatak (74°01′S, 70°38′W) on the Palmer Land plateau (Reference Peel, Mulvaney and DavisonPeel and others, 1988, fig. 2). Both cores exhibit an enrichment trend from 1970 to 1975 followed by increased depletion around 1975 or 1976. A core drilled in 1975 on Dolleman Island makes it possible to examine the 1970–75 event before substantial post-depositional modification (see dotted line in Reference Peel, Mulvaney and DavisonPeel and others, 1988, fig. 2). Again, the enrichment trend in the early 1970s is evident. The integration of these δ¹⁸Ο records, ranging along the length of the Antarctic Peninsula with the Siple Station record near the base, should provide a regional paleoclimatic record which is currently lacking.

Conclusions

Very distinct and well-preserved seasonal signals in δ¹⁸O and sulfate provide a means for confidently dating a deeper (302 m) core which should provide a 550 year paleoenvironmental history. The δ¹⁸Ο record is remarkably reproducible among four shallow cores and reflects reasonably well the principal features of two different Antarctic composite temperature trends (Fig. 6). The Siple Station δ¹⁸O record strongly reflects temperature trends at Faraday and is consistent with other isotopic records in the Antarctic Peninsula region.

The high accumulation (0.56 m a⁻¹ w.e.) leads to extremely low particulate concentrations. Coupled with the potentially excellent time-scale, the Siple Station dust record should provide a well-dated chronicle of major atmospheric turbidity events, such as sporadic or persistent periods of desertification, volcanic activity or increased entrainment of terrestrial material. Sulfate is primarily of non-sea-salt origin and seasonality is a function of available solar radiation which controls sulfate production. The annual sulfate flux exhibits large variability from 1966 to 1985 and may provide a tool for reconstructing Southern Hemisphere volcanic history. The predominant source of chloride at Siple Station is sea-salt aerosol, although it does not appear to be strongly influenced by conditions in the Weddell Sea sector. Nitrate concentrations agree with the levels found by other researchers in the Antarctic Peninsula region; however, a distinct annual concentration variation in nitrate is not found. Nitrate flux is higher during 1976–85 than that during 1971–75. The former encompassed that period when the Antarctic stratospheric ozone was found to be decreasing, but no direct link has been established. The longer chemical records forthcoming from the 302 m core should provide a valuable history of paleoenvironmental changes in the high southern latitude atmosphere.

Ultimately, the anticipated longer record must be integrated with other recent peleoclimatic histories including those from the Quelccaya ice cap, Peru (Thompson and others, Reference Thompson, Mosley–Thompson and Morales Arnao1984, Reference Thompson, Mosley-Thompson, Dansgaard and Grootes1986), James Ross Island, Dolleman Island and Gomez Nunatak in the Antarctic Peninsula. This will provide a valuable history for the southern middle to high latitudes where records are scarce.

Acknowledgements

We thank K. Mountain, for his participation in the field program, and the Polar Ice Coring Office of Lincoln, Nebraska, for conducting the drilling. We gratefully acknowledge the support services of the ITT-ANS contractor and especially L. DeGalen and B. Borden who oversaw the successful return of the ice core to The Ohio State University. We thank K. Doddroe for typing and R. Tope, S. Smith and T. Temple for illustrations. D. Lape and K. Najmulski designed and fabricated the firn sub-coring device. L. Klein and M. Davis conducted the particulate analyses. Their contribution to this work is gratefully acknowledged. This project was supported by U.S. National Science Foundation grant DPP-8410328 to The Ohio State University, and the oxygen-isotope analyses were supported by U.S. National Science Foundation grant DPP-8400574 to the University of Washington. This is contribution 674 of the Byrd Polar Research Center.