Background

Glacial strata in the Reedy Glacier area were first described by Reference MercerMercer (1968), who referred to lithified tills and glacigene strata unconformably overlying pre-Tertiary rocks as the Horlick Drift. Later, he described similar strata from Beard-more Glacier and proposed that they be called the Sirius Formation (Reference Mercer and AdieMercer, 1972) and he designated the Beardmore Glacier area as the stratotype. Subsequent work has defined numerous outcrops of the Sirius Formation along the Trans-antarctic Mountains between Reedy and Mackay Glaciers (e.g. Reference MayewskiMayewski, 1972, Reference Mayewski1975; Reference Mercer, Van Zinderen Bakker and RotterdamMercer, 1978, Reference Mercer, Hambrey and Harland1981, Reference Mercer1983). Initially, Reference MercerMercer (1968) proposed that these glacial deposits originated from local temperate glaciers in the Transantarctic Mountains. However, he later noted that only the elevated deposits I above c. 2200 m) seemed to originate from local temperate glaciers and that lower-elevation Sirius Formation deposits within present-day valleys along the Transan-tarctic Mountains were deposited by temperate outlet glaciers from the East Antarctic ice sheet (Reference Mercer, Van Zinderen Bakker and RotterdamMercer, 1978). Because of the wide distribution, distinctive lithofacies at different locations and potential for sub-division of Sirius Formation sequences, and to aid in interpretation of the multi-phase dcpositional history of these widely distributed deposits, Reference McKelvey, Webb, Harwood, Mabin, Thomson, Crame and ThomsonMcKelvey and others (1991) elevated the Sirius Formation to the Sirius Group.

In the early 1980s, marine diatoms from distinct Ceno-zoic biostratigraphic assemblages (including Pliocene) were recovered from the Reedy Glacier Sirius Group strata (Reference HarwoodHarwood, 1983) and later from other Sirius Group strata along the Transantarctic Mountains (Reference HarwoodHarwood and Webb, 1986b, 1991; Reference Harwood, Thomson, Crame and ThomsonHarwood, 1991. Reference Webb, Harwood, McKelvey, Mercer and StottWebb and others (1984) suggested that these diatoms and other microfauna and microflora originated from sedimentary basins (most likely, the Wilkes and Pensacola Subglacial Basins further inland from the Transantarctic Mountains. The diatoms were subsequently reworked into Sirius Group strata by glacial erosion, transport and deposition. The implication of this interpretation is that these sedimentary basins must have been marine seaways at times recorded by diatom flora productivity. These diatoms were subsequently recycled into the Sirius Group deposits. Hence,the East Antarctic ice sheet must have been reduced at various times in the Cenozoic (most recently in the Pliocene), and the East Antarctic ice sheet was more dynamic and sensitive to climate during the Cen-ozoic than previously suggested (e.g. Reference KennettKennett, 1977). Regardless of the implications for a dynamic glaciation of East Antarctica, the Pliocene microflora recycled into Sirius Group strata restrict the age of deposition of such Sirius Group sequences of the late Pliocene or younger.

This interpretation of a warmer and more dynamic glacial history of the Transantarctic Mountains was reinforced by the discovery of fossil wood (Nothofagus) and in-situ Nothofagus leaf mats (Reference CarlquistCarlquist, 1987; Reference Hill, Harwood and WebbHill and others, 1991; Reference Webb, Harwood, Alden, Mastrantonio and OdumWebb and Harwood, 1993; Reference Hill and TruswellHill and Truswell, 1993, Reference Francis and HillFrancis and Hill, 1996) within glaciolacustrine Sirius Group strata more than 1000ma.s.l. in the Beardmore Glacier area. Because the growth of Nothofagus required warmer temperatures than presently exist in the Beardmore Glacier area,Webb and others (1986,1994) suggested that the Nothofagus flora may have survived in coastal refugia and were subsequently uplifted. Uplift was later confirmed by Reference Webb, Harwood, Mabin and McKelveyWebb and others (1996) with the discovery of an in-situ foraminif-eral assemblage between c. 1100 and 1200 m a.s.l. in strata of the Cloudmaker Formation (Sirius Group), which is considered to underlie the Nothofagus- bearing beds of the Meyer Desert Formation (Sirius Group).

Currently, the interpretation of Sirius Group deposits along the Transantarctic Mountains is causing considerable debate. Some workers use strata from the Beardmore Glacier area (e.g. Reference Webb, Harwood, McKelvey, Mercer and StottWebb and others, 1984, Reference Webb1994, Reference Webb, Harwood, Mabin and McKelvey1996; Reference Webb and HarwoodWebb and Harwood, 1987; Reference McKelvey, Webb, Harwood, Mabin, Thomson, Crame and ThomsonMcKelvey and others, 1991) as their stratotype for interpretations regarding late Neogene glacial/tectonic and climate events that led to the deposition, sedimentary !content and present location of Sirius Group strata high in the Transantarctic Mountains. Their studies indicate a dynamic East Antarctic ice-sheet history and rapid recent uplift of the mountains in this region, with the most recent retreat of the ice sheet in the Pliocene. Other workers have used glacial drift deposits from high in the Transantarctic Mountains of southern Victoria Land as their stratotype for interpretations regarding the tectonic and paleoclimate significance of Sirius Group strata (e.g. Demon, and others, 1984, 1993; Reference Clapperton and SugdenClapperton and Sugden, 1990; Reference Stroeven, Prentice and BornsStroeven and others, 1992, Reference Stroeven, Prentice and Kleman1996; Reference Barrett, Blcakley, Dickinson, Hannah, Harper and RicciBarrett and others, 1997). These studies, along with a paleoclimate history of the Dry Valleys drawn from geomorphic surface development chronologically constrained by well-dated subaerial basalts and volcanic ash horizons (e.g. Reference Denton, Sugden, Marchant, Hall and WhichDenton and others, 1993; Reference Wilch, Lux, Denton and MclntoshWilch, 1993; Reference Marchant, Denton, Swisher and PotterMarchant and others, 1996), indicate stability of the late Neogene climate and ice sheet in East Antarctica and minimal uplift of the Transantarctic Mountains in the Dry Valleys area.

Setting

In the Reedy Glacier area, Sirius Group strata crop out at Metavolcanic Mountain,Tillite Spur and Quartz Hills, and the latter two localities are the subject of this paper. Reedy Glacier flows northwest, adjacent to the Wisconsin Range and is the most southerly outlet (85°-86°S) of the East Antarctic ice sheet through the Transantarctic Mountains (Fig. 1). It is flanked to the west by the Queen Maud Mountains and to the east by the Horlick Mountains, both of which rise to more than 3500 m a.s.l. The Queen Maud and Horlick Mountains consist of suites of Pre-Cambrian-Ordovician metamorphic and igneous rocks, non-conformably overlain by late Paleozoic Beacon Supergroup sediments (Reference Doumani and MinshewDoumani and Minshew, 1965; Reference MercerMercer, 1968).

In the upper Reedy Glacier area overlooking Tillite Spur, Sirius Group strata are exposed at c. 2500 m a.s.l. on the edge of the Wisconsin Plateau (Fig. 1). They form a 35 m sequence abutting the north wall of a small paleogla-cial valley and have a southerly aspect. The southern wall of the paleoglacial valley has been removed/destroyed during down-cutting by Olentangy Glacier, whose surface is about 500 m below Tillite Spur. Midway down Reedy Glacier at c. 1500 m a.s.l., Sirius Group strata at least 150 m thick overlie and infill a rugged topography of basement rocks at Quartz Hills. The base of the Sirius Group strata lie c. 90 m above the current Reedy Glacier surface and clearly pre-date the most recent down-cutting of Reedy Glacier. The best-exposed sequence infills a cirque near the southeastern end of Quartz Hills. Basal sediments of the Sirius Group sequence at Quartz Hills have been locally offset by small faults. The fault plains have well-developed slickensides and some quartzose mineralization.

Fig. 1. Map of the Reedr Glacier area, Antarctica, with the locations of Tillite Spur, Quartz Hills and other geographic features discussed in the text.

Tillite Spur Formation (new)

Here, we propose the name Tillite Spur Formation for the lithified diamictites and conglomerates that unconformably overlie pre-Tertiary rocks on the elevated flanks of the Wisconsin Plateau. These strata were originally described as Horlick Drift and subdivided into six informal units by Reference MercerMercer (1968) and later grouped by Reference MayewskiMayewski (1972) with similar strata from the Beardmore Glacier area and renamed Sirius Formation (Reference Mercer and AdieMercer, 1972). At Tillite Spur (the type section 1), the 35 m thick sequence consists of ten litholo-gical units (Fig. 2). The succession overlies a grooved and striated glacial pavement cross-cutting steeply dipping mudstones and sandstones of the Permian Weaver Formation (Reference MinshewMinshew, 1966). Units 1, 3, 5 and 8 are disconformity bounded, poorly sorted, massive to faintly stratified brown/olive-brown diamictites containing rounded to sub-rounded sedimentary and granitic claste. The upper surface of unit 1 is very weathered and contains deep desiccation cracks 3-5 cm wide. Unit 5 contains two thin undulating (10-30 cm) sheared olive-gray laminated mudstone horizons that are inclined locally at 20°. Units 2, 4, 6, 7 and 9 are disconformity bounded, poorly sorted, clast-supported conglomerates (using the classification scheme of Reference MoncrieffMoncrieff (1989)) containing mostly sub-rounded granitic clasts. Unit 10, the uppermost unit of the succession, is a 30 cm thick clast-supported conglomerate, with sub-rounded granitic clasts, that contains little to no matrix. In turn, it has been glaciated and is cross-cut by 3-5 cm deep west-trending glacial grooves (Fig. 3).

Quartz hills formation (new)

These strata were originally referred to as Stratified Drift by Reference MercerMercer (1968) and later grouped with the Horlick Drift into the Sirius Formation (Reference Mercer and AdieMercer, 1972). Here, we propose the name Quartz Hills Formation for the lithified diamictites and rhythmites (interbedded stratified mudstones and sandstones) that occur within the Reedy Glacier valley walls and unconformably overlie pre-Tertiary rocks. As defined, the formation is more than 100 m thick but the most continuous and representative sequence exposed at Quartz Hills is the lowermost 100 m of the formation. Here, we describe this and designate it as the type section. However, we note that further work will allow a more extensive composite section to be described for the entire sequence (>150 m) exposed at Quartz Hills. The sequence non-conformably overlies a grooved and striated undulating surface on coarse granites and Ferrar Dolerite, which has intruded the schistose rocks of the La Gorce Formation. The Quartz Hills Formation type section is subdivided into 18 lithological units (Fig. 4). Units 1, 3, 6, 9,11,13,16 and 18 are poorly sorted, gravelly, massive to indistinctly stratified, gray diamictites with erosional contacts. They contain common, sub-angular to well-rounded, striated granitic clasts. Unit 7 contains interbedded conglomerate and sandstones. The conglomerate matrices are locally muddy and sandy, and the sandstones are poorly sorted and contain occasional dropstones. Unit 15 is a sedimentary breccia. At Quartz Hills, it is 1.5 m thick but thickens in an up-valley direction. Units 8, 10, 12 and 14 are rhythmites (interbedded laminated mudstones and sandstones). Individual bed thicknesses vary between 1 and 50 mm, and sandier beds fine upwards and often grade into laminated mudstones. Stratification in the rhythmic sequences is commonly disrupted and sandstones often contain rip-up clasts of laminated mudstones from underlying beds. These units contain occasional dropstoncs. Unit 14 also contains 1-3 m thick lenses of diamictite. Units 2 and 4 are laminated, sandy mudstones without sandstone inter-beds. Unit 17 and the upper 2 m of unit 14 are strongly bio-turbated, sandy, micaceous mudstones, with occasional sand stringers, ripple-bed forms and sand-filled burrows.

Fig. 2. Stratigraphic column of the type section of the Tillite Spur Formation exposed at Tillite Spur. Additional graphic symbols are those standardly used in stratigraphic column description (e.g. Reference AndrewsAndrews, 1982). Fabric data are from 300 pebble AB plane measurements plotted on an equal-area stereographic projection azimuth (poles to plane) with a contour interval of 2% per 1 % area. Texture is graphed as weight per cent in φ intervals from combined dry-sieving and sedigraph analysis of the matrix fraction of samples. Weight percent coarser than 4φ is reported as coarse and weight per cent finer than 10φ is reported as rest.

Fig. 3. Glacial grooves cross-cutting Tillite Spur Formation (Sinus Group) strata at Tillite Spur. Surface depicted is inclined at 70°. Flow direction is from bottom left to top right. Handle of geologic pick is 1 m long.

Lithofacies

Rhythmite (interbedded laminated mudstones and sandstones)

This facies was only observed at Quartz Hills and comprises 24% of the sequence (Fig. 5c). Units of this facies are locally conformable with underlying strata or have loaded bases and overlie the underlying diamicts with erosional contacts. Individual mudstone beds are sandy, 1-30 cm thick and generally fine upwards. The upper part of the mudstone beds, when fine enough, are laminated on millimeter laminations and are occasionally convoluted or developed into flame structures from loading by overlying mudstones and sand-stones. Sandstone units also grade upwards. They are less common than the laminated mudstone horizons and generally have sharp unconformable bases often with small "rip-up" clasts from underlying laminated mudstone beds. They fine upwards into the laminated mudstone facies.

Fig. 4. Stratigraphic column of the type section of the Quartz Hills Formation exposed at Quarts Hills. Additional graphic symbols are those standardly used in stratigraphic column description (e.g. Reference AndrewsAndrews, 1982).Texture is graphed as weight percent in 1/2 φ intervals from combined dry-sieving and sedigraph analysis of the matrix fraction of samples. Weight per cent coarser than 4 φ is reported as coarse, and weight percent finer than 10φ is reported as rest.

Fig. 5. Examples of sedimentary facies from the Quartz Hills and Tillite Spur Formations: (a) a massive, poory sorted, matrix-supported, moderately sandy diamictite from the Tillite Spur Formation (unit 8). Handle of geologic pick is 1 m long; (b) a massive, poorly sorted, clast-supported, sandy conglomerate from the lower section of the Quartz Hills Formation (unit 6). Handle of geologic pick is 1 m long; (c) rhythmic interbedded laminated mudstones and sandstones from the Quartz Hills Formation (unit 8). Thicker sand interbeds are a sequence of sand ripples. Granite dropstone in right center of picture is 3 cm in diameter and deforms underlying beds by 1 cm. Overlying mud drapes have 1 cm of relief; (d) biolurbated sandy mudstone with occasional end sections of sand filled burrows visible from the upper section of the Quartz Hills Formation (upper part of unit 14). Knife blade is 7.5 cm long.

Bioturbated sandy mudstone

This facies was only observed at Quartz Hills and comprises 5% of the described sequence (fig. 5d). It is a massive, poorly sorted, micaceous, slightly gravelly, very sandy mudstone that is strongly bioturbated. Most stratification has been destroyed by the bioturbation. Occasional sand stringers and concave lenticular sand hummocks (fig. 6a) delineate a horizontal stratification. Some larger burrows are sand-filled and in unit 17 at Quartz Hills an identifiable burrow is preserved in outcrop (fig. 6b). The visible part of the burrow is 30 cm long, straight, gently dipping and contains a "turn-around" partway along its length and several 3 cm diameter interlocking chambers at its deepest extent.

Fig. 6. Sedimentary structures from unit 17 of the Quartz Hills Formation: (a) 3cm tall, concave lenticular sand hummocks; (b) 15 cm long sand-filled decapod burrow with a turn-around preserved towards the lefthand end; lower chambers in the center of the picture are c. 2.5cm across.

Micropaleontology

Siliceous microfossils

Siliceous marine microfossils have been recovered from 11 samples, ten (including three previously collected by Mercer) from Tillite Spur and a single sample previously collected by Mercer from Quartz Hills. Fifteen other samples (12 from Tillite Spur and three from Quartz Hills) were found to be barren of siliceous microfossils. Samples were prepared by disaggregation, sieving and various density-settling techniques as described by Reference HarwoodHarwood and others (1986). Siliceous microfossil assemblages recovered include marine diatoms (Fig. 7), silicoflagellates, chrysophycean cysts, radi-olarians, ebridians, freshwater diatoms, sponge spicules and pieces of marine sediment containing abundant diatoms. Ihe assemblage compositions in the sediment clasts are similar to the isolated diatoms, suggesting a common source. It is likely that the isolated diatoms were derived from disaggregation of the sedimentary clasts, which occurred during glacial transport or laboratory preparation.

Diatom abundances were generally very low (approximately 30 diatoms per sample) but five of the bulk samples from Tillite Spur yielded more than 50 diatoms per slide. Samples containing siliceous sedimentary microclasts were more productive than samples from which no microclasts were recovered. The most productive sample 64-JHM-70, collected from 15 m above the base of the Tillite Spur sequence (Fig. 2), contained diverse early Oligocene, Miocene and Pliocene marine diatom assemblages (Reference HarwoodHarwood, 1983, Reference Harwood1986). Of the marine species recovered, Rhizosolenia oligocae-nica, Sphynctolethus pacificus (fig. 7f), Stephanopyxis eocena and S. hyalomarginata are known from the late Eocene to the early Oligocene; Denticulopsis dimorpha (fig. 7k), D. simonsenii and D.lauta are Miocene: Fragilariopsis barronii, Thalassiosira inura (fig. 7d), T. fascicualata, T. kolbei and T. torokina (Fig 7a) are Pliocene to middle Pleistocene; T. insigna, T. Uulnifica (fig. 7e) and F praeinterfrigidaria (fig. 7j) are restricted to the Pliocene; and T. oliverana, T. lentiginosa (fig. 7c), F. kerguelensis and Actinocyclus actinochilus (fig. 7b) range from the Pliocene to recent. T. Uulnifica, F. kerguelensis and A. actinochilus are the youngest taxa identified. All first appear in the Southern Ocean and on the Antarctic shelf after 3.1 Myr (Reference Harwood, Maruyama, Wise and SchlichHarwood and Maruyama, 1992; Reference Winter, Harwood and RicciWinter and Harwood, 1997).

The only sample from Quartz Hills that yielded marine diatoms was 64-JHM-60 collected from line-grained strata close to the top of the sequence at Quartz Hills described here (Fig. 4). The diatom assemblage includes the Plio-Pleis-tocenc species Actinocyclus actinochilus, T. lentiginosa, T. oestrupii and T. torokina. Samples from units 8, 10 and 12 at Quartz Hills yielded only fresh-water diatoms. Sample 94QH47e contained well-preserved Stephanodiscus sp. (fig. 7g), which is a Neogene fresh-water form (Reference Bradbury, Krebs, Blome, Whalen and ReedBradbury and Krebs, 1995).

Fig. 7. Microfossils recovered from the Tillile Spur and Quartz Hills Formations, Sinus Group, Reedy Glacier area. Diatoms: (a) Thalassiosira torokina Brady, Quartz Hills Formation, sample 64JHM60; 100 μm diameter. (b) Actinocyclus actinochilus (Ehrenberg) Simonsen, Quartz Hills Formation, sample 64JHM60; 90 μm diameter, (c) Thalassiosira Ienti-gjnosa (fanisch) Fryxell, Tillite Spur Formation, sample 64JHM70; 100 μm diameter. (d) Thalassiosira inura Gersonde, Tillite Spur Formation, sample TS-2, 30 μm diameter, (e) Thalassiosira vulnifica (Gombos) Fenner, Tillite Spur Formation, 64JHM70, 50 μm diameter, (f) Sphynctolethus pacificus (Hajos) Sims, Tillite Spur Formation, 64JHM70,45 μm diameter, (g) Stephanodiscus sp., Quartz Hills Formation, sample 64JHM47e, 75 μm diameter. (h) Thalassionema nitzschoides var. parva Heiden, Tillite Spur Formation, sample TS-ll, 20 μm long, (i) Thalassionema nitzschioides (Grunow),Tillite Spur Formation, sample TS-7, 25 μm long. (j) Fragilariopsis pracinterfrigidaria (McCollum), Tillite Spur Formation, sample 64JHM70, 45 μm long. (k) Denticulopsis dimorpha Schrader, Tillite Spur Formation, 64JHM70,55 μm long. Palynomorphs: (i) Protohaploxypinussp. (taeniate bisacate) pollen, sample TS-26, 64 μm long. (m) Podocarpidites sp. pollen, Quartz Hills Formation, sample QH-105, 52 l μm diameter.

Discussion

The diamicts of the Tillite Spur Formation record two ice sources. The gray conglomerates were deposited by an alpine glacier, that flowed west across Tillite Spur and was locally fed from a catchment on the Wisconsin Plateau. This glacier may have carved the palco-valley within which the Tillite Spur Formation sits and then later deposited the gray conglomerates. Striae on the palco-valley floor and pebble fabric demonstrate that the glacier flowed westward from the Wisconsin Plateau. The finer-grained, matrix-supported, brown-olive diamictites are weakly imbricated. The imbrication demonstrates that they were deposited by northward-flowing ice, most likely the paleo-Reedy Glacier, when it flowed at higher levels, or alternatively when the Wisconsin Plateau region was at a lower elevation.

The conglomerates sourced from the Wisconsin Plateau have a low proportion of fine particle sizes. There are several possible reasons for this: (1) the units may have been deposited by cold, dry alpine ice that did not produce many fines, 2 the glacier had warmer ice and fines which were winnowed during deposition, or (3) it may be a result of the granitic source bedrock material. Diamictites of the paleo-Reedy Glacier ice contain a high mud content and the units are stratified, suggesting that the sediment is not from a local source. We interpret the alternating sequence of diamictites and conglomerates in the Tillite Spur Formation to represent glacial-interglacial cycles with ice-deriving sediment, alternately from nearby alpine sources, and more distal Reedy Glacier palco-valley sources, respectively.

The exposure face of the Tillite Spur Formation exhibits glacial grooves from a more recent glacial episode.This was perhaps related to the initial down-cutting by Olentangy Glacier, which responded in turn to the most recent down-cutting phase of Reedy Glacier to its current level.

The diatoms recovered from the Tillite Spur Formation are from the finer-grained matrix-supported brown-olive diamictite units deposited by the northward-flowing palco-Reedy Glacier. Imbrication measurements from this study support the hypothesis of Reference Webb, Harwood, McKelvey, Mercer and StottWebb and others (1984) that these marine flora are sourced from the Pensacola Basin to the south behind the Transantarctic Mountains.They represent phases of reduction in the East Antarctic ice sheet at times of marine productivity and subsequent erosion, transport and redeposition into the glacigenic strata deposited by the paleo-Reedy Glacier within the Tillite Spur Formation of the Sirius Group. Paleogene palynomorphs identified in this study must also have originated from south of the Transantarctic Mountains.

In the Quartz Hills Formation, we interpret the finely stratified/rhythmic interbedded mudstones and sandstones (units 8,10,12 and 14) to have been deposited in a proglacial lake. We conclude that these deposits are lacustrine, because only fresh-water diatoms were recovered from these beds and, while rhythmic and relatively undisturbed sequences with minimal or no organic matter, have been documented in marine settings (Reference Mackiewicz, Powell, Carlson and MolniaMackiewicz and others, 1984), they are also indicative of lacustrine settings (Reference SchluchterSchluchter, 1979). We also suggest that they were deposited in a lake that occupied much of the paleo-Reedy Glacier valley because, if the lake only occupied the area of the paleo-cirque, sedimentation would have been dominated by lodgement to proximal glacial sediments derived from a Reedy Glacier ice margin. Nearby glacial activity is indicated by dropstones in the stratified glacial units (units 8, 10, 12 and 14) (Fig 5c) and interbedded coarse conglomerate and diamictite units (units 7, 9,11,13 and 14) (Fig 5a and b). We interpret the fining-upwards lensoid coarse sand to conglomerate units with rip-up clasts and a scoured base to be turbidite deposits from a local glacial ice margin.The massive finer-grained matrix supported diamictites. we interpret to have been deposited as lodgement tills when the ice margin advanced and grounded across the proglacial lake. We suggest these alternating stratified sequences and thick massive tills represent glacial interglacial cycles in the Quartz Hills Formation. They are interpreted as advance and retreat episodes of the paleo-Reedy Glacier, respectively, covering and re-exposing a large proglacial lake. At this stage, we are uncertain of the relationship between the glacial interglacial cycles in the strata at Quartz Hills and Tillite Spur.

The introduction of burrowing organisms into the upper part of the sequence at Quartz Hills is marked by the very pronounced bioturbation in the uppermost unit 14, and throughout unit 17 (Fig. 4). Lower in the sequence, similar rhythmic strata are devoid of bioturbation. The sand-filled burrows observed in unit 17 were produced by a decapod (personal communication from R. Feldmann, 1997). The burrows are unlined, inclined and have an outer diameter of c. 10 mm. They have an open framework, are infilled by material of a different texture to the surrounding matrix and the networks contain turn-arounds, branches and terminal chambers, all features which are indicative of decapods from shallow neritic and littoral environments (cf. Reference Weimer and HoytWeimer and Hoyt, 1964; Reference Frey and MayouFrey and Mayou, 1971; Reference Griffis and SuchanekGriffis and Suchanek, 1991; Reference MyrowMyrow, 1995). Given the cold and essentially vegetation-free environment indicated by the Quartz Hills sequence, we conclude that terrestrial migration of burrowing organisms and introduction into this previously organism-free environment is unlikely. Therefore, the lake must have been close lo sea level and the burrowing (including decapod) life forms were introduced into the environment by a marine incursion. Given the nature of the burrows and the sedimentary associations, we also hypothesize (from comparison with modern-day occurrences (Reference Weimer and HoytWeimer and Hoyt, 1964; Reference Frey and MayouFrey and Mayou, 1971) that these organisms lived close to the berm. This conclusion means that the lowest bioturbated horizon in the Quartz Hills Formation is also a sea-level datum in the sequence. This horizon now sits at about 1600 m a.s.l., indicating significant uplift since their deposition.

The only age constraint available for both the Tillite Spur and Quartz Hills Formations is the Pliocene diatom flora.This flora was suggested as having been reworked into the Sirius Group strata from marine sedimentary basins now behind the Transantarctic Mountains, beneath the East Antarctic ice sheet (Reference Webb, Harwood, McKelvey, Mercer and StottWebb and others, 1984). Their incorporation into the glacial strata provides a maximum age of Middle Pliocene for the Tillite Spur Formation and may provide a direct age for shallow fiordal sediments in the upper units of the Quartz Hills Formation, if the flora are "in-situ” at this location. However, recent studies have demonstrated that some diatoms can be reworked on to exposed geologic surfaces in Antarctica by eolian processes (Reference Burckle and PotterBurckle and Potter, 1996; Reference Kellogg and KelloggKellogg and Kellogg, 1996; Reference Stroeven, Prentice and KlemanStroeven and others, 1996; Reference Barrett, Blcakley, Dickinson, Hannah, Harper and RicciBarrett and others, 1997), and it has recently been hypothesized that the diatoms may have been emplaced on exposed geologic surfaces in Antarctica as impact ejecta fall-out (Reference GersondeGersonde and others, 1997).

Several factors suggest that the diatom flora in the Tillite Spur and Quartz Hills Formations were introduced into the strata at the time of deposition rather than by subsequent eolian or impact processes: (1) several age-restricted floras are present, necessitating a source containing strata of diverse ages. Such a source is not currently exposed for eolian deflation on the Antarctic craton; (2) an Eocene -Oligocene marine flora is relatively abundant in one sample only from the Tillite Spur Formation. Other occurrences are not uniform in abundance or age ranges of taxa recovered; (3) numerous samples are barren of diatom flora and not uniformly distributed at the surface; (4) sample 64-JH-70 contains abundant flora (more than 50 diatoms per slide, compared to two- three diatoms per slide for wind-blown marine diatoms (Reference Burckle and PotterBurckle and Potter, 1996), or a few diatoms per cm² for ejecta fall-out (Reference GersondeGersonde and others, 1997), that we feel must have originated from marine sedimentary clasts or in the case of the Quartz Hills Formation may represent an "in-situ" marine occurrence; (5) in the Tillite Spur and Quartz Hills Formations, samples are dominated by marine floras, whereas samples used to demonstrate eolian processes are dominated by fresh-water and marine coastal flora (Reference Kellogg and KelloggKellogg and Kellogg, 1996; Reference Barrett, Blcakley, Dickinson, Hannah, Harper and RicciBarrett and others, 1997; Reference GersondeGersonde and others, 1997); (6) our samples were collected from strata exposed in eroding, near-vertical cliff faces (with no weathering of the exposed face and no diagenetic modification or intergranular mobility behind the eroding face) rather than on altered sub-horizontal geologic surfaces (Reference Stroeven, Prentice and KlemanStroeven and others, 1996; Reference Barrett, Blcakley, Dickinson, Hannah, Harper and RicciBarrett and others, 1997); (7) several diatomaceous sediment clasts (illustrated in Reference HarwoodHarwood (1986)) are more than 100 μm in diameter —a size too large to be wind-blown or penetrate the diamicton (Reference Burckle, Gayley, Ram and PetitBurckle and others, 1988).

Conclusions

The Tillite Spur and Quartz Hills Formations are two very different sequences of the Sirius Group. The Tillite Spur Formation strata are thin and non-stratified, and similar in appearance to Sirius Group sediments described from the Dry Valleys area (Reference MayewskiMayewski, 1975; Reference Brady and McKelveyBrady and McKelvey, 1979, Reference Brady and McKelvey1983). They were deposited in an alpine elevated glacial setting in the Transantarctic Mountains (Reference Mercer, Van Zinderen Bakker and RotterdamMercer, 1978) and represent alternating intramontane and trunk-valley basin sediments similar to the model proposed by Reference WebbWebb (1994). Quartz Hills Formation strata are more similar in appearance to Cloudmaker Formation strata from the Beardmore Glacier region (Reference Webb, Harwood, Mabin and McKelveyWebb and others, 1996). The Quartz Hills Formation strata were deposited in a lacustrine/fiord setting and represent advance and retreat in a trunk-valley delta basin system similar to the model proposed by Reference WebbWebb (1994). Such a setting is much lower in elevation than that envisaged for the Tillite Spur Formation.

The Tillite Spur and Quartz Hills Formations record advances of a paleo-Reedy Glacier. Both formations are Pliocene or younger but it is not known whether they are temporal equivalents. Recycled marine diatom flora (some in clasts) in the diamictites were deposited by an advanced paleo-Reedy Glacier. The diatom flora record several episodes of marine deposition behind the Transantarctic Mountains (the source of the glacigene Tillite Spur and Quartz Hills formation sediments) during times in the Cenozoic when this area of the Antarctic interior must have been ice-free (cf. Reference Webb, Harwood, McKelvey, Mercer and StottWebb and others, 1984). Marine strata in the upper units of the Quartz Hills Formation indicate at least 500 m Myr ^l of uplift of the Queen Maud Mountains of the Transantarctic Mountains since middle Pliocene times. More recently, Reedy Glacier and associated glaciers have down-cut at least 500 m. in response to the Pliocene-Pleistocene uplift, and exposed the Sirius Group strata described here. These strata were probably not exposed until the middle-late Pleistocene.

Three orders of paleoclimatic variability are recorded in the Sirius Group strata from Rccdy Valley: (1) recycled marine microfloras in glacial diamictites indicate intervals of marine incursion into the Antarctic cratonic interior co-occurring with reductions in the East Antarctic ice sheet; (2) an advancing and retreating paleo-Reedy Glacier deposited a glacial-interglacial sequence alternating on a 10-100 kyr scale; (3) centimeter and millimeter stratification in strata of the Quartz Hills Formation record annual kyr scale variability. As yet, we do not understand the temporal relationships of the Tillite Spur and Quartz Hills formations (except that they are both middle-late Pliocene in age). However, Reedy Glacier represents an important place to investigate the relationship between high-altitude alpine facies and lower-elevation trunk-valley (marine) facies of the Sirius Group strata as they both crop out in the same valley system. Such a study should significantly improve our understanding of the paleocevironmental and paleoclimatic significance of Sirius Group strata in different and disconnected geographical and temporal settings. However, as is made clear from this study, interpretations of one Sirius Group outcrop should not be imposed on other geologically and geographically different outcrops of Sirius Group strata.