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Polar ice is an important component of the modern climate system, affecting global sea level, ocean circulation and heat transport, marine productivity, air-sea gas exchange, and planetary albedo, among others. The modern semipermanent ice caps are, geologically speaking, a relatively young phenomenon. Since mid-Permian (~270 Ma) times, parts of Antarctica became reglaciated only ~34 m.y. ago, whereas full scale, permanent Northern Hemisphere continental ice began only 2.7 to ~3 m.y. ago (e.g., Zachos et al., 2008) (Fig. F1). In a broad sense, the record of Antarctic glaciation from the time of first ice sheet inception (presumed to incept around the Eocene/Oligocene boundary; Oligocene isotope Event 1 [Oi-1] glaciation; e.g., Miller et al., 1985) through the significant periods of climate change during the Cenozoic, such as the Oligocene/Miocene boundary, the Miocene isotope Event 1 (Mi-1) (e.g., Miller et al., 1985), the mid-Miocene climatic optimum, late Neogene cooling, early Pliocene warming events, the Quaternary glacial–interglacial cycles, and the concomitant biotic and paleoceanographic evolution, is not only of scientific interest but also is of great importance for society. State-of-the-art climate models (e.g., DeConto and Pollard, 2003a, 2003b; Huber et al., 2004; DeConto et al., 2007; Pollard and DeConto, 2009) combined with paleoclimatic proxy data (e.g., Pagani et al., 2005) suggest that the main triggering mechanism for inception and development of the Antarctic ice sheet were the decreasing levels of CO2 (and other greenhouse gas) concentrations in the atmosphere (Figs. F1, F2) and that the opening of critical Southern Ocean gateways (e.g., Kennett, 1977; DeConto and Pollard, 2003a, 2003b; Huber et al., 2004; Barker and Thomas, 2004) played only a secondary role. With current rising atmospheric greenhouse gases resulting in rapidly increasing global temperatures (Intergovernmental Panel on Climate Change [IPCC], 2007;, studies of polar climates are prominent on the research agenda. Understanding Antarctic ice sheet dynamics and stability is of special relevance because, based on IPCC (2007) forecasts, atmospheric CO2 doubling and a 1.8°–4.2°C temperature rise is expected by the end of this century. The lower values of these estimates have not been experienced on our planet since 10–15 Ma, and the higher estimates have not been experienced since before the ice sheets in Antarctica formed (Fig. F3).

Since their inception, the Antarctic ice sheets appear to have been very dynamic, waxing and waning in response to global climate change over intermediate and even short (orbital) timescales (e.g., Wise et al., 1991; Zachos et al., 1997; Barker, Camerlenghi, Acton, et al., 1999; DeConto and Pollard, 2003a, 2003b; Pollard and DeConto, 2009). Yet, not much is known about the nature, cause, timing, and rate of processes involved. Past ocean drilling into the Antarctic continental shelf and basins in Prydz Bay and the Ross Sea (i.e., Ocean Drilling Program [ODP] Legs 119 and 188, Deep Sea Drilling Program [DSDP] Leg 28, and Cape Roberts Project) indicates two basic states of the Antarctic ice sheets: (1) an early phase lasting from ~34 to ~14 Ma with a less stable ice cover characterized by strong cyclic waxing and waning (O’Brien et al., 2001; Barrett, 2009; Zachos et al., 1997, 2008; Wade and Pälike, 2004; Pälike et al., 2006) and (2) a later (from ~14 Ma to recent) phase when deep-sea isotope records (e.g., Miller et al., 1985; Flower and Kennett, 1994) indicate that the Antarctic ice sheets became a quasipermanent and more stable feature sustaining polar climates. However, even these “stable” ice sheets may have varied considerably in size, perhaps by as much as 25 m of sea level equivalent (SLE) (Kennett and Hodell, 1993; Pollard and DeConto, 2009; Naish et al., 2009). Of the two main ice sheets, the West Antarctic Ice Sheet (WAIS) (Fig. F4) is mainly marine based and is considered less stable. The East Antarctic Ice Sheet (EAIS), which overlies continental terrains that are largely above sea level, is considered stable and is believed to respond only slowly to changes in climate. However, reports of beach gravel deposited 20 m above sea level in Bermuda and the Bahamas from 420 to 360 ka indicate the collapse of not only the WAIS (6 m of SLE) and Greenland ice sheet (6 m of SLE), but possibly also 8 m of SLE from East Antarctic ice sources (Hearty et al., 1999). Therefore, during episodes of global warmth, with likely elevated atmospheric CO2 conditions, the EAIS may contribute just as much or more to rising global sea level as the proverbial unstable Greenland ice sheet. In the face of rising CO2 levels (IPCC, 2007), a better understanding of the EAIS dynamics is therefore urgently needed from both an academic as well as a societal point of view.

A key region for analysis of the long- and short-term behavior of the EAIS is the eastern sector of the Wilkes Land margin, located at the seaward termination of the largest East Antarctic subglacial basin, the Wilkes subglacial basin (Fig. F5) (Drewry, 1983; Ferraccioli et al., 2001, 2007, 2009). The base of the portion of the EAIS draining through the Wilkes subglacial basin is largely below sea level, suggesting that this portion of the EAIS can potentially be less stable than other areas of the EAIS. Numerical models of ice sheet behavior (e.g., Huybrechts, 1993; DeConto and Pollard, 2003a, 2003b; DeConto et al., 2007; Pollard and DeConto, 2009) (Fig. F2) provide a basic understanding of the climatic sensitivity of particular Antarctic regions for early ice sheet formation, connection and expansion, and eventual development of the entire ice sheet. For example, in these models glaciation is shown to have begun in the East Antarctic interior, discharging mainly through the Lambert Graben to Prydz Bay. These models imply that the EAIS did not reach the Wilkes Land margin until a later stage. These models must now be validated through drilling and obtaining concrete evidence from the sedimentary record. Sediments from Prydz Bay cores drilled during Leg 188 (O’Brien, Cooper, Richter, et al., 2001; Cooper, O’Brien, and Richter, 2004) provided records from the Late Cretaceous and early late Eocene preglacial and relatively warm climates to the full glacial conditions of the Pliocene–Pleistocene. Like at Prydz Bay, the timing and mode of the onset of glaciation at the Wilkes Land Continental Margin is still unknown but is essential for providing age constraints for models of EAIS development and changes in its volume. Moreover, detailed portrayal of the subsequent Cenozoic history and dynamics of the Antarctic glacial cycles at Wilkes Land will provide further constraints for model experiments and future predictions about EAIS stability.

Conceivably even more important than the history of the Antarctic glaciations are past lessons of deglaciations and periods of exceptional warmth. Seismic surveys and pilot studies indicate that the Wilkes Land margin also includes sites of ultrahigh accumulation rates of sediments recording the Holocene deglaciation and subsequent climate and sedimentological variability extending over the past 10,000 y. One of the expedition objectives was to recover and analyze a unique ~200 m sequence of likely annually layered sediments. These seasonally laminated (tree ring style) deposits consist predominantly of phytoplankton remains and potentially constitute one of the world’s most expanded archives of environmental change extending through the Holocene. We also planned to core several sequences from the Pleistocene and Pliocene that formed during interglacial intervals of exceptional warmth, periods that may provide valuable information about Antarctica’s response to warming predicted in the centuries ahead.