Introduction
An increasing number of parameters of climatic significance are being determined in ice cores, providing a record of past conditions. The obtained data are relevant to boundary conditions prescribed by an atmospheric global circulation model (GCM) and for the validation of output results. Reciprocally, GCM calculations could help to assess tile validity of some of the interpretations of the ice-core records which are not straightforward, and to connect and extend high-latitude changes to a much larger scale. The late-glacial maximum (LGM) is of particular interest for palaeoclimatic GCM reconstructions.
In central areas of the ice sheet, one ice record from West Antarctica (Byrd) and two from East Antarctica (Vostok, Dome C) extend back to the LGM. Such a period is also covered by a few drillings in the coastal area of East Antarctica (Law Dome, Terre Adelie) but in such sites the climatic records are highly disturbed by ice-flow effects. In this paper we review climatic LGM-Holocene changes inferred from inland ice records in Antarctica; information about ice-thickness changes will also be discussed for coastal drillings.
Due to the present lack of adequate absolute-dating techniques, the time scale of the ice records has been obtained by ice-flow model calculations. Although it is not possible to determine very accurate ages in this way, the chronologies proposed for the central Antarctic ice cores are in sufficient agreement to characterize the LGM and Holocene stages and to compare the obtained climatic records.
Atmdspheric Data
Temperature from isotope climatic records
The δ18O isotope shifts associated with the LGM-Holocene transition (Figs.1, 2 and 3) are about 7‰ for Byrd (Reference Johnsen, Dansgaard, Clausen and LangwayJohnsen and others 1972), 5‰ for Vostok (Reference Barkov, Korotkevich, Gordienko and KotlyakovBarkov and others 1977) and 5.4‰ for Dome C (Reference Lorius, Merlivat, Jouzel and PourehetLorius and others 1979). An interpretation in terms of temperature changes is complicated because the isotopic composition of the precipitation is governed not only by Its temperature of formation TF but also depends on the origin and history of the air masses, on the condensation processes involved, and on its altitude of formation. The mean δ18O content of modern precipitation decreases with mean surface temperature TS, and a very well-fitted linear relationship (r = 0.989) is observed from −22 to −55°C over East Antarctica with a gradient of 0.75‰ °c−1 (Reference Lorius and MerlivatLorius and Merlivat 1977). This and other facts (Reference RobinRobin 1977) suggest the possibility of reconstructing past temperatures from isotopic data. A simple isotopic model recently developed (Jouzel and Merlivat to be publishedFootnote *) suggests that the influence of the altitude of formation of the precipitation is negligible and that the effect of the sea-water temperature in the vapour source area may be small at least for Inland stations. Due to supersaturation over ice, snow is formed out of isotopic equilibrium and the calculated δ180/TF gradient shows a rather constant value of about 1.2‰ °c−1. As suggested by Reference RobinRobin (1977), TF is rather close to the temperature TI prevailing above the thin inversion layer, while the inversion strength is linearly related to TS, with dTI/dTS = 0.67 (Reference Lorius, Merlivat, Jouzel and PourehetLorius and others 1979). A theoretical value of 0.8‰ °c−1 is thus inferred for d δ18O/dTS, a figure very close to the experimental gradient (0.75‰) observed over East Antarctica. This good agreement leads us to use this theoretical value for a tentative estimation of past temperature changes although there are obvious insufficiencies in this approach (i.e. the model is based on ideal isolated air masses and there is no available experimental gradient over West Antarctica); further improvements may be expected from the simulation of isotopic cycles with GCMs (Reference Joussaume, Sadourny and JouzelJoussaume and others 1984[b], in which changes in the source area and in the dynamic history of the air masses can be taken into account, and from further data obtained concerning the present δ distribution, in particular in West Antarctica.
The Dome c record. Smoothed δ180 (‰) (from Reference Lorius, Merlivat, Jouzel and PourehetLorius and others 1979), dust and marine Na concentrations (from Reference De Angelis, Jouzel, Lorius, Merlivat, Petit, Raynaud and BergerDe Angelis and others in press, Reference Royer, De Angelis and PetitRoyer and others in press), deuterium excess d (from Reference Jouzel, Merlivat and LoriusJouzel and others 1982), and CO2 concentrations (individual measurements and running means, adapted from Reference Delmas, Ascencio and LegrandDelmas and others (1980)) plotted versus age and depth (m of ice).
The Byrd record. δ18O (‰), aluminium and microparticle content, total Na and
concentrations, total gas V, and CO2 content versus age and depth. δ18O (‰) and the chronology are from Reference Johnsen, Dansgaard, Clausen and LangwayJohnsen and others (1972); the δ values versus depth provided by W Dansgaard have been smoothed using a spline function. Microparticle (greater than 0.62 μm per 500 μl sample) content is from Reference ThompsonThompson (1977). Al, Na and
values: circles are from Reference Cragin, Herron, Langway, Klouda and DunbarCragin and others (1977), points are from Reference Ragone and FinelliRagone and Finelli (1972), Δ are surface compiled values from Reference BriatBriat (1974). V results are from Reference Raynaud and WhillansRaynaud and Whillans (1982); the difference between lines (1) and (2) for the LGM ice indicates that the Byrd area was lower than at present by about 175 to 205 m (from the ΔE scale given in the figure). CO2 concentrations are from Reference Neftel, Oeschger, Schwander, Stauffer and ZumbrunnNeftel and others (1982) and Reference Neftel, Oeschger, Schwander, Stauffer and ZumbrunnOeschger and others (1982).
The Vostok record. δ180(‰) from Reference Kotlyakov and GordiyenkoKotlyakov and Gordiyenko (1982) and total gas content V versus depth and age from Korotkevich and others (to be publishedFootnote *). For the V record a scale in terms of elevation change is also given; the difference between dashed lines 1 and 2(ΔE ≈ − 30 m) indicates that the LGM ice was formed at an elevation close to the current Vostok altitude.
The observed LGM-Holocene isotopic shifts must first be corrected for the increase (1.6‰) in the mean δ18O content of oceanic waters during the LGM (Reference Duplessy and GribbinDuplessy 1978). The corrected isotopic changes are then 8.6‰ for Byrd, 6.6‰ for Vostok and 7‰ for Dome C, leading to respective TF changes of about 7, 5.5 and 6°C. These values refer to low troposphere conditions, above the inversion layer, while the derived surface temperature TS changes are about 10 and 8 to 9°C.
These tentative estimated temperature values may include effects linked with changes in the ice-formation site and in ice-sheet surface topography. As discussed in another section, very low velocity and ice-thickness changes suggest that these effects may be very small for central East Antarctica sites although for West Antarctica (Byrd), LGM ice may originate from a distance of about 100 km. The Antarctic isotopic records from central areas therefore seem mainly to reflect atmospheric temperature changes; this is further supported by the comparison of the δ profiles which show not only the same trends and comparable amplitude for the LGM-Holocene transition, but have also recorded the same significant shorter-term events, which are more likely climatic features than ice-sheet dynamic effects. As also previously pointed out (Reference Lorius, Merlivat, Jouzel and PourehetLorius and others 1979), the climatic history of the last 30 ka thus inferred from ice cores is in fact in very good agreement with available southern hemisphere proxy data. Further support of our estimated temperature changes comes from ice crystal-size changes (Reference Duval and LoriusDuval and Lorius 1980) with depth. The decrease observed during the LGM-Holocene transition can in fact be interpreted by surface temperature changes which affected the crystal growth; the estimated temperature variation for Dome c is in very good agreement with the one inferred from the δ record (Petit and others to be publishedFootnote **).
Relative humidity over the ocean from isotope records
It was recently suggested (Reference Lorius, Merlivat, Jouzel and PourehetMerlivat and Jouzel 1979) that, when considering two different periods, the variation of the deuterium excess in precipitation (d = δD – 8 δ18O) can be used to estimate the variation of the relative humidity h over the source region of the precipitating air mass. A theoretical approach can be used to discuss the possible influence of various factors and indicates that d is linearly dependent on h (Reference Jouzel, Merlivat and LoriusJouzel and others 1982); with d = 10 (the mean value of modern precipitation), an h value of 81% is inferred which is very close to the value that actually prevails over the ocean surface. The main feature of the d profile obtained from the Dome C ice core (Fig.1) is the gradual change of 4.5‰ between the LGM and 7.5 ka BP. This shift has been interpreted (Reference Jouzel, Merlivat and LoriusJouzel and others 1982) as reflecting a higher value of h over ocean areas providing moisture for Antarctica (south of 40°S), estimated around 90% for LGM conditions through ⋄d = – 45 ⋄h. We keep in mind that there are many assumptions in the derivation of this relationship; nevertheless similar changes may have also affected the tropical and equatorial regions (Reference Lorius, Merlivat, Jouzel and PourehetMerlivat and Jouzel 1979, Reference Flohn and BergerFlohn 1981). Its possible hemispheric and even global significance must still be confirmed, both by further experimental data and by GCM simulation of LGM climate.
Marine aerosol concentration changes have been connected with wind intensity U over oceanic source areas (Reference Petit, Briat and RoyerPetit and others 1981). The correlation observed between d and Na concentration (Fig.1) thus suggests a link between h and U. It has been proposed (Reference Jouzel, Merlivat and LoriusJouzel and others 1982) that this link results from the constant value of U(1–h) for LGM and Holocene conditions, inferred from evaporation flux and energy-balance considerations. An increase of 10% for h then also suggests an increase in the wind speed over the oceanic source area by a factor of about 2 during the LGM, in agreement with the figure obtained from marine aerosols.
Snow accumulation
Due to the present lack of adequate absolute dating techniques and of convincing results on seasonal changes of geochemical parameters for deep ice, there is no direct evidence of changes in snow accumulation A. At Dome C, favourable glaciological conditions suggest that the time scale is linearly related to 1/A. Direct determination of A in the surface layers and the comparison of the ice isotopic record with a suitable 14C-dated (Reference Duplessy, Moyes and PujolDuplessy and others 1980) marine isotopic profile from the Indian Ocean was used to estimate that A remained rather constant over the Holocene but decreased with a colder climate, the accumulation 14 ka BP being about 75% of the present value (Reference Lorius, Merlivat, Jouzel and PourehetLorius and others 1979). Since then the validity of this assumption has been confirmed, with a further check on the obtained chronology, by the existence of continental dust indexes about 26 and 13 ka BP (Fig.1) attributed to the beginning and end of an aridity period (14C dated) over southern hemisphere continents (Reference BowlerBowler 1976). As suggested by Reference RobinRobin (1977), the accumulation appears to be primarily governed by the amount of water vapour that can be carried in the air mass above the inversion. The temperature changes deduced above would imply a decrease of about 40% for Dome c and Vostok, and of about 60% for Byrd. However this reduction may be partially compensated by the increase in air fluxes over Antarctica during the LGM as discussed in this paper. GCM simulations would help to clarify the scarce evidence of climate related accumulation changes over Antarctica.
Aerosols
From theoretical considerations (Reference Junge and MoralesJunge 1979) and experimental determinations (Reference Pourchet, Pinglot and LoriusPourchet and others 1983) it is generally assumed that the concentration of impurities in the precipitation is directly related to the concentration in the atmosphere. This assumption, which should be further investigated, is the basis for reconstructing past aerosol data from ice-core records. The three Antarctic ice cores show very large changes over the last 30 ka (Reference Cragin, Herron, Langway, Klouda and DunbarCragin and others 1977, Reference Petit, Briat and RoyerPetit and others 1981, Reference Thompson and Mosley-ThompsonThompson and Mosley-Thompson 1981, Reference De Angelis, Jouzel, Lorius, Merlivat, Petit, Raynaud and BergerDe Angelis and others in press) with very large values around the LGM which cannot be explained by possible accumulation changes.
Elemental determinations (Si, Al) and scanning electron microscope observation and analysis indicate an influx of dust at this time which is mainly of continental origin (Reference Cragin, Herron, Langway, Klouda and DunbarCragin and others 1977, Reference Petit, Briat and RoyerPetit and others 1981, Reference Briat, Royer, Petit and LoriusBriat and others 1982) even if the Byrd core shows many ash layers which may have a local volcanic origin. The LGM/Holocene ratio is 4 for Byrd, 24 for Vostok and 17 for Dome C. The high LGM dust value has been interpreted as reflecting both the extension (x 5) of arid continental sources in the southern hemisphere (Reference SarntheinSarnthein 1978) due to a dry environment (CLIMAP Project Members 1981) and stronger winds. Antarctic 1ce cores, therefore, probably record record large-scale environmental changes; the high elevations of Dome C (3 240 m) and Vostok (3 420 m) suggest that they are more representative than Byrd (1 500m) of the background atmospheric dust which travels at elevations higher than 3 000 m in the troposphere (Reference Delany, Pollock and ShedlovskyDelany and others 1973), although the dust repartition may not be homogeneous over all Antarctica. Assuming a constant snow accumulation and a dust flux over the high East Antarctic plateau proportional to the flux over the sources, an increase in wind velocity by a factor of about 1.4 has been calculated for the source areas (Reference Petit, Briat and RoyerPetit and others 1981). This is a maximum value since the transport efficiency which is linked to turbulence has also played a role as demonstrated by the presence of microparticles as large as 10 μm in LGM ice samples (Reference Petit, Briat and RoyerPetit and others 1981). Such a wind velocity increase is probably connected with an increase in the temperature gradient with latitude during the LGM (CLIMAP Project Members 1981) over the southern hemisphere.
Marine aerosol concentrations are also higher during the LGM (see Na in Fig.1) with LGM/Holocene ratios of about 2 to 3 for Byrd (Reference Cragin, Herron, Langway, Klouda and DunbarCragin and others 1977), 4 to 5 for Vostok (Reference De Angelis, Jouzel, Lorius, Merlivat, Petit, Raynaud and BergerDe Angelis and others in press) and 5 for Dome C (Reference Petit, Briat and RoyerPetit and others 1981). These higher values may also be explained by an increase in the wind over the Southern Ocean (40 to 50°S wind belt), with the effect of the sea-ice extension during the LGM (CLIMAP Project Members 1981) compensated by a higher transport efficiency. The comparison of Na and δ18O profiles (Fig.1) shows that marine aerosol concentrations increase as climate gets colder; they both probably reflect Antarctic and sub-Antarctic changes. Differences between sites for the LGM/Holocene ratios may tentatively be explained by deeper penetration of cyclonic disturbances associated with a higher meridional temperature gradient during the LGM (Reference De Angelis, Jouzel, Lorius, Merlivat, Petit, Raynaud and BergerDe Angelis and others in press).
The main ionic constituents such as sulphate and nitrate also show higher concentrations during the LGM. The increase for
, about × 1.5 at Byrd (Reference Cragin, Herron, Langway, Klouda and DunbarCragin and others 1977) and about 2 to 3 for East Antarctic sites (M Legrand in preparation), is likely to be associated with an increase in the marine contribution. Legrand also found a threefold increase for nitrates in LGM Dome C ice samples. Assuming that the concentrations measured in the ice reflect atmospheric changes, LGM aerosol concentrations were then higher by about × 5 to 6 (Reference Royer, De Angelis and PetitRoyer and others in press).
The high aerosol loading of the LGM atmosphere has probably affected the radiation balance. A tentative estimate (Reference Royer, De Angelis and PetitRoyer and others in press) suggests a warming effect over Antarctica smaller than 2°C and a relative heating rate significantly higher over the dust sources, e.g. tropical desert areas. This suggests a possible significant change in one of the boundary coriditions, i.e. the atmospheric composition, prescribed in atmospheric GCM palaeoclimatic simulations.
Antarctic ice cores have recorded significant changes of aerosol concentrations in the regional low troposphere. A three-dimensional picture over Antarctica and reconstitution up to the source areas may not be achieved without the help of atmospheric circulation models (Reference Joussaume, Rasool, Sadourny and PetitJoussaume and others 1984[a]); the ice-core data may potentially be used as a check on such simulations. A significant increase (by a factor of 2.5) in concentration of the cosmogenic 10Be has also been observed in the LGM Dome C samples with respect to rather constant Holocene values (Reference RaisbeckRaisbeck and others 1981). The climatic implications are not clear at present as such a change may be related to various parameters, i.e. snow accumulation, atmospheric exchanges, primary cosmic-ray and geomagnetic field intensity, and solar activity.
Carbon dioxide (CO2
When firn turns into ice, atmospheric air is entrapped as bubbles. Using appropriate gas-extraction procedures (Reference Raynaud and WhillansRaynaud and others 1982) it is possible to obtain, from cold ice cores, a record reflecting the past evolution of the atmospheric CO2 content. Although different processes may complicate the interpretation of the CO2 measurements in air bubbles in ice (Reference Lorius, Raynaud, Bach, Crane, Berger and LonghettoLorius and Raynaud 1983), this method provides the most direct evidence for such an atmospheric record.
For the record extending back to the LGM, the most relevant Antarctic data was obtained from the Dome C and Byrd cores (Reference Delmas, Ascencio and LegrandDelmas and others 1980, Reference Neftel, Oeschger, Schwander, Stauffer and ZumbrunnNeftel and others 1982). Although there is significant scatter in the data which could reflect both experimental problems and natural fluctuations, the following features are clearly apparent: CO2 values for the LGM are of the order of 200 ppmv; for the Holocene period the records indicate a mean figure of about 270 ppmv (Figs.1 and 2). These values are consistent with the results obtained from other ice cores (Reference Delmas, Ascencio and LegrandDelmas and others 1980, Reference Neftel, Oeschger, Schwander, Stauffer and ZumbrunnNeftel and others 1982). More recent measurements performed on both cores indicate that between about 800 and 2 500 a BP, which is before the significant anthropogenic perturbation of the atmospheric CO2, the CO2 concentration was of the order of 260 ppmv (Reference Barnola, Raynaud, Neftel and OeschgerBarnola and others 1983). This figure should be compared with the CO2 concentration measured in the atmosphere since 1958, which is today around 340 ppmv. A new study of the D57 core (East Antarctica suggests a value of about 260 ppmv around 1850 AD and the existence of slight natural variations before this time (Reference Raynaud and BarnolaRaynaud and Barnola 1984).
Thus, according to ice-core data, important changes have occurred in the CO2 atmospheric reservoir since the LGM; the same relative increase is observed with very different climatic changes: the first increase (from 200 to 270 ppmv) is linked with the drastic LGM-Holocene climatic change and the second (from 260 to 340 ppmv) corresponds to a period with relatively stable temperature conditions.
If the CO2 change measured in the atmosphere between 1958 and today is mainly attributed to the effect of the fossil fuel consumption, causes for earlier variations are more difficult to assess. Part of the change that has occurred since the 260 ppmv level, which could be representative of the pre- 1850 AD atmosphere, may be due to a biospheric CO2 source induced by mankind before the use of fossil fuel (Reference Lorius, Raynaud, Bach, Crane, Berger and LonghettoLorius and Raynaud 1983, Reference Raynaud and BarnolaRaynaud and Barnola 1984). On the other hand the increase in the CO2 concentration, which occurred between the LGM and the Holocene period, was forced by natural mechanisms. Recent explanations involve changes in the marine biological productivity (Reference BroeckerBroecker 1982, Reference McElroyMcElroy 1983) or in the reef-building activity (Reference BergerBerger 1982) linked with the sea-level rise following the melting of the ice sheets; possible modification in the oceanic circulation may also play a primordial role (Reference Broecker and TakahashiBroecker and Takahashi 1984, Reference Stauffer, Hofer, Oeschger, Schwander and SvegenthalerStauffer and others 1984). A precise study of the comparative timing between the CO2 and climate changes inferred from ice-core records may provide important information in this respect. New results obtained from the Dome c core suggest that the interpretation of this comparative timing near the end of the LGM could be complex because of the “stepped” shape of the CO2 variation (Reference Raynaud and BarnolaRaynaud and Barnola 1984).
Ice-Thickness Data
The total gas content V in ice depends theoretically on the atmospheric pressure p and temperature T, and on the ice-pore volume VC when the firn turns into ice (Reference RaynaudRaynaud 1977). Reference Raynaud and LebelRaynaud and Lebel (1979) found an experimental relationship between V and the elevation E of the ice-formation site under present conditions:
v[cm3 g−1 of ice] = −1.66 × 10−5 Em + 0.138
This equation implies that VC decreases linearly with temperature and we can assume that the variations of V with E are only due to the changes of P and T according to:
(Reference Raynaud and LebelRaynaud and Lebel 1979). At constant pressure, V would then decrease as the temperature decreases at a rate of about 2 X 10−4 cm3 g−1 of ice per °C. Although the physical mechanisms causing the Vc−Tc dependence are not clearly understood, application of the above empirical figures is the most direct way to obtain information about past ice-surface elevation.
The application to LGM conditions first requires a correction for changes in T which can be obtained, as previously discussed, from isotopic shifts. An uncertainty remains with regard to possible changes of the atmospheric pressure field which could, in particular, be connected with different circulation patterns. Due to the lack of information, which could probably be obtained from atmospheric palaeo-simulations, we will assume in our interpretations that the elevation-pressure pattern did not change with time.
When the elevation of the ice-formation site is thus obtained, we have to assess ice-flow conditions so that the past surface elevation may be reconstructed, which will , in turn, reflect the past ice thickness. For the Byrd ice core, Reference Raynaud and WhillansRaynaud and Whillans (1982) calculated the expected V profile from steady-state conditions, i.e. assuming a surface elevation profile constant with time, upstream from Byrd station. Note that the “steady-state” line (1) in Figure 2 is slightly different from the one given by Raynaud and Whillans because a surface temperature change of 10°c (as discussed previously) linked to the termination of the LGM has been used instead of a value of 7°c. Figure 2 indicates a significant deviation between the “steady-state” curve and the V experimental results in the depth interval corresponding to the LGM. This deviation suggests that the surface elevation at the ice formation site, estimated to be at about 100 km upstream from the drilling site (Reference WhillansWhillans 1979), was lower than present by about 175 to 205 m. Keeping in mind the limitations of this method, the gas information strongly suggests that the ice thickness around Byrd did not change dramatically at the same time that the last ice age ended. The gas evidence is consistent with another study based on the interpretation of internal radio echo layers (Reference WhillansWhillans 1976). The behaviour of the Byrd area between the LGM and present conditions may be typical of the central area of West Antarctica.
For the central part of East Antarctica the only available data including the LGM comes from the Vostok core (Korotkevich and others to be publishedFootnote *). Although the experimental procedure used lacks accuracy, the results suggest that the LGM ice was formed at an elevation close to the current Vostok altitude. From ice velocities at the order of a few metres per year (Reference Raynaud, Lorius, Budd and YoungYoung 1979) and the present day surface elevation contours, we can estimate that the LGM ice was formed a few tens of kilometres from the present drilling site at an elevation which was about 100 m lower than the current one. The Vostok gas results are consistent with the interpretation of the temperature profile measured in the Dome c bore hole (Reference Ritz, Lliboutry and RadoRitz and others 1982). They both suggest a slight thickening of this central part of East Antarctic since the end of LGM but, in any case, no dramatic change.
The interpretation of the combined V-δ obtained from ice cores drilled in some East Antarctica coastal sites is less straightforward, due to the significant ice-flow effects. Nevertheless, results from the D–10 (66°40’S 140°01’E) core in Terre Adélie suggest that the surface elevation about 250 km from the present coast was of the order of 400 m higher during the LGM than now (Reference Raynaud and LebelRaynaud and others 1979, Reference Young, Raynaud, De Angelis, Petit and LoriusYoung and others 1984). other V results from the Cape Folger F core suggest that the ice-thickness change for the area of the Law Dome near Casey (66°17’S 110°32’E) was even larger (Reference Budd and MorganBudd and Morgan 1977, Reference LebelLebel 1979).
In conclusion, the interpretation of the limited available V data indicates a possible slight thickening of the central parts of the ice sheet and a more significant thinning of some coastal areas in East Antarctica since the LGM. This picture differs from the one given by some reconstructions (e.g. Reference Hughes, Denton, Andersen, Schilling, Fastook, Lingle, Denton and HughesHughes and others 1981), based on ice-sheet modelling, which conclude a much thicker West Antarctica during the LGM. A slight thickening of central West Antarctica between the LGM and the Holocene could have been induced by an increase in the rate of snow accumulation (Reference Raynaud and WhillansRaynaud and Whillans 1982), an explanation which could also hold for central East Antarctica. On the other hand, coastal areas could have thinned between the LGM and the present under the influence of the sea-level rise and the temperature increase.
However much more experimental data and ice-sheet modelling efforts are required to sort out a realistic picture of Antarctic ice surface elevation changes since the last ice age.
Conclusion
The review of available Antarctic ice-core data from inland sites and covering both Holocene and LGM suggests very drastic modifications of the atmospheric environment. Some have a regional significance; the proposed temperature and suggested accumulation changes could provide useful comparisons with GCM results. Others may have impact on a hemispheric scale (aerosol concentrations, relative humidity over the ocean); the inferred changes for the wind velocity and relative humidity could again be checked with atmospheric model outputs. Aerosols may have changed the radiation balance and when feasible should be included as prescribed boundary conditions in model simulation. This also applies to carbon dioxide, as the large changes recorded in Antarctic ice are of a global significance and may have played, through strong interactions between continents, atmosphere and oceans, a major role in the LGM-Holocene climatic change. In contrast with the drastic modifications of the atmospheric environment, ice-core data suggest only slight changes in central Antarctic ice thick-nesses since the LEM, but more pronounced changes in the coastal areas; central and marginal areas of the ice sheet could have reacted differently to the climatic change.
