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 We reconstructed subsurface (∼45–200 m water depth) temperature variability in the eastern Antarctic continental margin during the late Holocene, using an archaeal lipid-based temperature proxy (TEX86L). Our results reveal that subsurface temperature changes were probably positively coupled to the variability of warmer, nutrient-rich Modified Circumpolar Deep Water (MCDW, deep water of the Antarctic circumpolar current) intrusion onto the continental shelf. The TEX86Lrecord, in combination with previously published climatic records, indicates that this coupling was probably related to the thermohaline circulation, seasonal variability in sea ice extent, sea temperature, and wind associated with high frequency climate dynamics at low-latitudes such as internal El Niño Southern Oscillation (ENSO). This in turn suggests a linkage between centennial ENSO-like variability at low-latitudes and intrusion variability of MCDW into the eastern Antarctic continental shelf, which might have further impact on ice sheet evolution.
 An important clue towards the potential future impact of Antarctic warming on glaciological changes can be obtained from past temperature records beyond the instrumental period. To properly address Antarctic's climate variability and its relationship to the global climate system in relation to natural forcing, it is essential to investigate temperature records beyond the instrumental period. The number of Holocene quantitative temperature records from ice cores [Stenni et al., 2010], from the southern hemisphere (SH) mid-latitude [Hodell et al., 2001; Bianchi and Gersonde, 2004; Nielsen et al., 2004; Kaiser et al., 2008], and from the continental margin of the western Antarctic Peninsula [Shevenell et al., 2011] has increased substantially in recent years. However, quantitative temperature records from the eastern Antarctic continental margin are still lacking since reconstructions based on diatom-based transfer functions, one of the most widely used techniques in the Southern Ocean to decipher sea surface temperature (SST), are not sensitive enough for quantitative temperature reconstruction for the coastal Antarctic [Crosta et al., 2008]. Here we overcome this obstacle by applying an archaeal membrane lipid-based paleothermometer (TEX86L) for the Polar Oceans [Kim et al., 2010], a modified version of the initial TEX86 [Schouten et al., 2002], to estimate ocean temperatures in the eastern Antarctic continental margin.
2. Material and Methods
 We obtained Holocene climate records from piston core MD03-2601 (66°03.07S; 138°33.43E; 746 m water depth,Figure 1), recovered from the slope of one of the depressions composing the Dumont d'Urville Trough off Adélie Land retrieved during the MD130 Images X cruise (CADO-Coring Adélie Diatom Oozes) with R.V. Marion Dufresne II [Denis et al., 2009]. The Dumont d'Urville Trough is located along the East Antarctic coast in the eastern Indian sector of the Southern Ocean (see Figure S1 in the auxiliary material). This area is influenced by several water masses and currents [Bindoff et al., 2000; Lacarra et al., 2011; Williams et al., 2010]: (1) the wind-driven East Wind Drift, also called Antarctic Coastal Current, which flows westward and transports Antarctic Surface Water that can be subdivided into Summer Surface Water and Winter Water; (2) the MCDW at depths of ∼200–800 m, which intrudes onto the shelf region and provides a reservoir of nutrient-rich, warmer water that subsequently upwells into the upper water column; and (3) the High Salinity Shelf Water, formed by brine-rejection during winter sea ice formation and cooling of the MCDW, which flows northward as part of the Adélie Land Bottom Water. The age model of the core [Denis et al., 2009] was based on seven Accelerator Mass Spectrometry (AMS) 14C dates of the humic fraction of bulk organic matter which were calibrated into calendar ages using Calib 5.0 using a reservoir age of 1300 years. The Probosciadiatom counts were performed at a ∼10–20 years resolution. For the glycerol dibiphytanyl glycerol tetraether (GDGT) analysis, the sediment core was sampled on average at 180-year intervals. Sediments were freeze-dried, homogenized, and extracted as described byKim et al. .The extract was separated into an apolar, ketone, and polar fractions with Al2O3 column chromatography using hexane:DCM (9:1 v/v), hexane:DCM (1:1 v/v), and DCM:MeOH (1:1 v/v), respectively. The polar fractions were filtered using a 0.4 μm PTFE filter and analyzed with a high performance liquid chromatography-atmospheric pressure positive ionization-mass spectrometer (HPLC-APCI-MS) as described bySchouten et al. . The TEX86L was calculated and converted into SSTs according to Kim et al. . All the samples were analyzed in duplicate with average analytical error being ±0.2°C (±1σ).
3. Results and Discussion
 TEX86Lwas developed based on the strong relationship between the distribution of thaumarchaeotal isoprenoid GDGTs and satellite-derived annual mean SST using a global core-top dataset [Kim et al., 2010]. However, marine Thaumarchaeota, producing the membrane lipids used for TEX86L, occur throughout the whole water column [e.g., Karner et al., 2001] and thus thaumarchaeotal GDGT-based temperature proxies may potentially integrate temperatures over a wide depth range (seeauxiliary material). The TEX86L-derived temperatures may reflect predominantly epipelagic (approximately 0–200 m water depth on a global scale) temperatures because of the more efficient food web-based scavenging of thaumarchaeotal cells [e.g.,Wuchter et al., 2005]. Furthermore, Thaumarchaeota are virtually absent in the Antarctic summer surface water (the ∼0–45 m layer of low salinity water mass) in contrast to their elevated abundances in winter in a ∼45–105 m interval of cold, salty water (i.e., the summer remnant of the previous winter, surface-mixed layer) [Kalanetra et al., 2009]. Therefore, we hypothesize that TEX86L predominantly reflects subsurface (the depth interval ∼45–200 m) temperatures rather than SST. Consequently, we established a new calibration of TEX86Lwith depth-integrated annual mean temperatures from 0 to 200 m water depth (Figure 2). The calibration error is ±2.8°C, which is a systematic error, comprises many factors which are globally variable but at a single locality it will be of less importance or less variable [cf. Tierney et al., 2010]. Thus, relative temperature variations within the TEX86L record will have a much lower error compared to absolute temperature estimates.
 Temperature reconstructed from TEX86L values of surface sediments derived from equation (S3) in Text S1was on average 4.0°C (n = 2) at our core site, which is higher than the depth-integrated (0–200 m) annual mean temperature value of −0.2°C from the WOA09 [Locarnini et al., 2010] but reasonable considering the calibration error. TEX86L-derived temperatures varied between 0°C and 4°C over the Holocene (Figure 3a). The most striking features of our TEX86L record are 1) a prominent increase in temperature centred at 6 kyr BP and 2) substantial temperature variability during the Late Holocene. Our TEX86L record (Figure 3a) does not show clear long-term cooling or warming trends which would be anticipated from orbitally driven insolation forcing (Figure 3b) [Berger and Loutre, 1991; Renssen et al., 2005]. The TEX86L temperature variations also differ from those of temperature proxy records from other regions (Figure S3). In general, SH high-latitude records derived from diatom abundances (Figures S3a–S3c) infer a Mid Holocene warming and a subsequent cooling since 3–4 kyr BP for both the Antarctic Peninsula [Taylor et al., 2001] and East Antarctica [Denis et al., 2010]. In contrast, SH mid-latitude records [Bianchi and Gersonde, 2004; Crosta and Shemesh, 2002; Nielsen et al., 2004] depict a general cooling until 4–5kyr BP (Figures S3d–S3f) and a subsequent warming (Figure S3d) or SST stabilization (Figure S3e). Temperature records inferred from Antarctic ice cores (Figures S3g and S3h) also demonstrate dissimilar Holocene variations between sites (ΔTsite, SH high-latitude signals) and moisture sources (ΔTsource, SH mid-latitude signals) [Stenni et al., 2010].
 To explore physical mechanisms associated with subsurface temperature variability at our core site, we extracted anomalies of the annual mean temperatures of water masses at 30 m, 163 m, and 1225 m for the area 60–65°S, 135–145°E from the LOVECLIM coupled atmosphere–sea ice–ocean–vegetation model experiment, forced by annually varying orbital parameters, greenhouse gas concentrations, and Laurentide Ice Sheet deglaciation [Renssen et al., 2010]. We selected these water depths in the model output because they provide a good representation of the surface-mixed layer, subsurface, and deep water masses, respectively. Surface and sub-surface simulated temperatures mimic Holocene climate evolution inferred from diatoms [Crosta et al., 2008] while deep simulated temperatures are different than Holocene surface climate evolution. The simulated temperatures at all water depths (Figure 3c) show a pronounced peak at around 6 kyr BP in phase with a warming event recorded in the TEX86L record (Figure 3a). The reason for this pronounced maximum in the model calculation is that around 6 kyr BP, after complete recession of the Laurentide Ice Sheet, deep convection in the Labrador Sea became active, leading to greater North Atlantic Deep Water (NADW) flux and warmer NADW, which in turn warmed up Southern Ocean waters from below [Renssen et al., 2010]. This warming of the deep water masses around 6 kyr BP is best seen in the simulated temperatures at 1225 m water depth (Figure 3c, blue curve). Return to cooler Southern Ocean conditions after 5.5 kyr BP was associated with the orbitally-forced cooling of the Southern Ocean and the source region of NADW in the Nordic and Labrador Seas [Renssen et al., 2005, 2010]. Enhanced subsurface temperature variability during the Late Holocene as revealed by the TEX86Lrecord is also apparent for the simulated surface and sub-surface temperatures but is less evident in simulated deep water temperatures. Poor representation of glacier dynamics and impacts in Antarctic coastal areas in the climate model for the Late Holocene on centennial time scales may have obscured variability of surface and sub-surface simulated temperatures [Denis et al., 2009].
 For a coupling of subsurface temperature variability recorded by TEX86L (Figure 3a) with warmer, nutrient-rich MCDW intrusion at our core site comes from the Setae diatom group (S-DG;Corethronpennatum, ChaetocerosPhaeoceros spp., and Rhizosolenia spp. counts from Denis et al. , Figure 3d) and the Proboscia spp. (P. inermis, P. truncate, and P. alata, Figure 3e, see also Figure S4; this study). Today, the S-DG group develops in summer and shows a clear preference for nutrient-rich, well-mixed waters in relation to katabatic winds [Beans et al., 2008]. As intrusion of MCDW onto the continental shelf is induced by wind-induced Ekman pumping, the S-DG record at our core site probably indicates intensification of summer wind mixing and nutrient input since 3.5 kyr BP [Denis et al., 2010]. The Probosciaspp. record in core MD03-2601 showed a similar long-term Holocene pattern with a general decrease between 10 and 5.5 kyr BP followed by an increase. This is in good agreement with a recent study in the western Antarctic Peninsula that, based on biomarkers forProboscia diatoms showed increased Proboscia diatom productivity in shelf waters of the northwestern Antarctic Peninsula during the late Holocene in response to intensification of MCDW upwelling [Willmott et al., 2010]. This suggests that more frequent intensification of MCDW upwelling over the depth interval >∼100 m might have resulted in the observed warmer subsurface TEX86L temperatures during the Late Holocene.
 Intriguingly, during the period of higher TEX86L-derived temperature variability (Figure 3a) and thus inferred more frequent, intensified intrusions of MCDW into the upper water column, sea ice over ice-free conditions during the growing season prevailed as shown by the ratio betweenFragilariopsis curta and Fragilariopsis kerguelensis (Fc/Fk ratio, Figure 3f) [Denis et al., 2009]. This seemingly contradictory pattern between increased sea-ice cover and warmer temperature conditions during the Late Holocene can, however, be explained by the sea ice and temperature seasonal dynamics in the study area. The Late Holocene (i.e., Neoglacial period) was shown to experience greater late winter and early spring sea ice concentrations than the Mid Holocene (i.e., Hyperthermal period) [Crosta et al., 2008; Pike et al., 2009], which was favorable to the production of small Fragilariopsis species [Beans et al., 2008]. After sea ice disintegration, more intense wind activity during summer [Steig et al., 2000; van Ommen et al., 2004] may have promoted greater surface water mixing and upwelling of MCDW favorable to the production of S-DG [Denis et al., 2010] and Proboscia diatom species. Upwelling of MCDW also resulted in warmer subsurface temperatures recorded in the TEX86L-derived temperature (Figure 3a).These sea ice and atmospheric seasonal dynamics have thus caused a simultaneous increase in sea ice related diatom (a spring record) and S-DG andProboscia spp. (summer records) abundances during the Late Holocene at our core site.
 Our TEX86Lrecord indicates that more frequent subsurface temperature changes with large amplitude at siteMD03-2601 was coincident with higher climate variability on a global scale during the Late Holocene [Mayewski et al., 2004]. During this period, the ENSO conditions at low-latitudes [Moy et al., 2002; Cane, 2005] were linked to orbitally induced changes in insolation seasonality (Figure 3g). The northward movement of the SH westerly wind belt with the reduction of zonal winds in its core zone in southernmost Chile [Lamy et al., 2010] and abrupt fluctuations in sea temperature in the western Antarctic Peninsula [Shevenell et al., 2011]are in good agreement with more El Niño-like conditions during the Late Holocene. Presently, low to high-latitude teleconnections are recognized in ENSO-sea ice relationships in the western Antarctic Peninsula region [Stammerjohn et al., 2008]. Similarly, centennial-scale variability of subsurface temperatures in East Antarctica was probably coupled to the Late Holocene development of ENSO variability through wind variability along the eastern Antarctic coastal zone which impacted seasonal dynamics of upwelling intensity, SST, and sea ice extent. The proposed interaction between ENSO and subsurface conditions in East Antarctica should be further assessed with higher resolution TEX86L records.
 We present a Holocene ocean temperature record obtained from the eastern Antarctic continental margin using the archaeal membrane lipid-based paleothermometer (TEX86L) for the Polar Oceans. Our study showed that TEX86L-derived temperatures at our core site reflect a subsurface signal rather than surface. Interestingly, our TEX86Lrecord does not show clear long-term cooling or warming trends but higher temperature variability during the Late Holocene. We hypothesise that this late Holocene temperature variability was linked to the intensification of MCDW intrusion onto the eastern Antarctic continental shelf in association with the centennial ENSO-like variability at low-latitudes. More TEX86L subsurface temperature records with higher temporal resolution will allow to elucidate the natural variability of MCDW intrusion to the inner continental shelf around Antarctica, which drives thinning and acceleration of glaciers [Thoma et al., 2008] and will potentially further improve our knowledge of Antarctic ice sheet evolution, and its consequences for global environmental changes.
 We would like to thank J. Ossebaar and M. Kienhuis at NIOZ for analytical supports and F. Taylor (University of Tasmania) and B. Stenni (University of Trieste) for providing data. This paper was written during JHK's stay at EPOC, as an invited scientist funded by the INSU-CNRS in France. SS and VW were supported by a VICI grant from the Netherlands Organisation for Scientific Research. The research leading to these results has received funding from the European Research Council under the European Union's Seventh Framework Programme (FP7/2007-2013) / ERC grant agreement . XC was funded by INSU-CNRS TARDHOL and ESF Polar Climate HOLOCLIP projects (HOLOCLIP publication 6).
 The Editor thanks two anonymous reviewers for their assistance in evaluating this paper.