Four repeat hydrographic sections across the eastern Weddell gyre at 30°E reveal a warming (by ~0.1°C) and lightening (by ~0.02–0.03 kg m−3) of the Antarctic Bottom Water (AABW) entering the gyre from the Indian sector of the Southern Ocean between the mid-1990s and late 2000s. Historical hydrographic and altimetric measurements in the region suggest that the most likely explanation for the change is increased entrainment of warmer mid-depth Circumpolar Deep Water by cascading shelf water plumes close to Cape Darnley, where the Indian-sourced AABW entering the Weddell gyre from the east is ventilated. This change in entrainment is associated with a concurrent southward shift of the Antarctic Circumpolar Current's (ACC) southern boundary in the region. This mechanism of AABW warming may affect wherever the ACC flows close to Antarctica.
 The meridional overturning circulation is a key mechanism by which the ocean transports heat, carbon, and other climatically important tracers around the planet [e.g., Ganachaud and Wunsch, 2000]. Production of dense bottom water (collectively named Antarctic Bottom Water, AABW) at a few specific high-latitude regions of the Southern Ocean constitutes an important part of this circulation. AABW formation is driven by seawater density modification through air-sea-ice interactions near the Antarctic margins [Orsi et al., 1999] that are sensitive to climatic forcing.
 AABW has experienced pronounced property changes in recent decades. Purkey and Johnson [2010, 2012] report widespread warming and volumetric contraction of AABW across much of the global ocean abyss since the 1980s. AABW formed in the Ross Sea and off Adélie Land freshened by, respectively, ~0.01 between the late 1960s and the 1990s [Jacobs et al., 2002; Rintoul, 2007; Jacobs and Giulivi, 2010] and ~0.03 between the mid-1990s and the mid-2000s [Aoki et al., 2005; Rintoul, 2007]. This has been tentatively linked to shelf water freshening [Jacobs et al., 2002; Jacobs and Giulivi, 2010], possibly resulting from the accelerated mass loss of the West Antarctic Ice Sheet by enhanced basal melting [Pritchard et al., 2012].
 Here we expand upon the evidence for climatic changes in AABW properties by documenting a remotely induced warming of the AABW entering the Weddell gyre from the Indian sector of the Southern Ocean. Exploring the likely mechanisms for this change, we find that a southward migration of the ACC's southern boundary off the Cape Darnley/Prydz Bay region may have brought relatively warm mid-depth waters closer to the continental shelf edge, where they are entrained by cascading dense shelf water.
2 Data Sets and Methods
 Four repeats (1993, 1996, 2006, and 2008) of conductivity-temperature-depth (CTD) profiles along section I6S at 30°E between 61.5°S and 68°S (Figure 1) collected during the World Ocean Circulation Experiment and CLIVAR (Climate Variability and Predictability) programs were obtained via the CLIVAR and Carbon Hydrographic Data Office (http://cchdo.ucsd.edu). Additional hydrographic data and Argo float profiles were obtained from the Southern Ocean (http://woceatlas.tamu.edu/Sites/html/atlas/SOA_DATABASE.html) and Argo database (ftp://ftp.ifremer.fr/ifremer/argo), respectively. Neutral density (γn, kg m−3) and dynamic height (dyn m) were derived. We define AABW as water with γn > 28.27, after Orsi et al. . For display, salinity (S) data from 1993 and 1996 were vertically smoothed with a 20 dbar running mean.
 Weekly satellite snapshot sea surface height (SSH) maps (from TOPEX/Poseidon, Jason 1 and 2, ERS-1 and -2, Envisat, GFO) were obtained for the eastern Weddell gyre region (55°S–65°S, 30°E–90°E) from Archiving, Validation, and Interpretation of Satellite Oceanographic Data [Le Traon et al., 1998]. Inter- and multiannual SSH changes were quantified using a least squares linear regression for sea ice-free months (January–May) from 1996 to 2008.
 CFC-11 and CFC-12 concentrations were analyzed for the 1993, 1996, and 2008 transects and used to calculate transit ages [after Klatt et al., 2002]. A transit time distribution (TTD) analysis of the section CFC core elicited information about advection (as transit times, the time for an atmospheric perturbation to be transmitted from the ventilated surface to an ocean interior location) and mixing (as age distributions and source water fractions). Transit ages were optimized through a least squares residual minimization between observed and calculated concentrations across a range of age dispersion values (which describe the advection (Γ)/mixing (Δ) relationship) [after Waugh et al., 2003]. An age dispersion of 2 years (signifying a relatively advective core) was used, but results were similar for values between 1 and 8.
 AABW properties between 61.5°S and 68°S along 30°E exhibit significant spatiotemporal variability. Similar profiles were grouped empirically (Figure 2) by the (green) absence or presence of a (black) stronger or (red) weaker deep CFC maximum and distinct θ-S characteristics. Latitudinal extents of the groups varied by less than 1.5° between surveys. In 1993 and 1996, θ-S properties are homogeneous (Figures 2a and 2b) and AABW exhibits a deep CFC maximum at γn ~ 28.37 (Figure 3a), suggesting recent ventilation, as noted by Archambeau et al. . However, in 2006 and 2008 (Figures 2c and 2d), in addition to the first AABW type present at the northernmost stations (Figure 2, green), another is found farther south near the shelf break, with lower salinity (Figure 2, black), a larger θ-S spread, and a lighter CFC maximum (γn ~ 28.34, Figure 3a). The γn shift of the black group's CFC maxima between the 1990s and 2000s corresponds to lightening of about 0.02–0.03 kg m−3. Further, the black profiles inflect toward the green at γn = 28.36 in 2006 and 2008 (Figures 2c and 2d), and show lower CFC concentrations (Figure 3a), suggesting that this lighter AABW flows over an older bottom layer. Our results indicate that, whereas in the 1990s, this bottom water had no distinct thermohaline signal, in the 2000s, it had a clear θ-S signature not documented previously (Figures 2c and 2d). Figures 3b and 3c reveal a translation in the CFC-θ profile but not in CFC-S: the CFC maximum shifts from approximately θ = −0.5°C in the 1990s to θ = −0.4°C in 2008. Therefore, the 0.02–0.03 kg m−3 AABW lightening is induced by a 0.1°C change in temperature rather than salinity.
 The deep CFC maximum observed in AABW near the continental slope at 30°E suggests recent ventilation in the region of Prydz Bay [e.g., Jacobs and Georgi, 1977; Archambeau et al., 1998]. Indeed, the nearby Cape Darnley polynya (69°E) was recently shown to be a significant source of new bottom water, contributing 13%–30% of Atlantic sector AABW production, although the role of the Amery Ice Shelf could not be dismissed [Ohshima et al., 2013]. The CFC-11 and CFC-12 concentrations observed at 30°E between 1993 and 2008 (Figure 3, CFC-12 not shown) within the Indian sector-sourced AABW indicate transit times of 6–9 years, although θ-S anomalies can propagate more rapidly [Waugh and Hall, 2005]. These divergent estimates are probably due to differing atmospheric histories. Using the Cape Darnley area as the ventilation source, the transit time implies velocities in reasonable agreement with near-bottom velocities observed along the shelf break between Prydz Bay and 30°E (~0.05 ms−1) [Meijers et al., 2010], indicating minimal influence of AABW varieties from other sources.
 Our observations suggest that a warming, rather than a freshening, of the Indian sector-sourced AABW is the dominant cause of its lightening. This warming could be caused by changes in: (1) source region shelf water properties; (2) the flux of heat to cascading shelf water plumes via a change in the temperature and/or rate of entrainment of relatively warm, mid-depth Circumpolar Deep Water (CDW); or (3) the rates of advection or mixing of the newly formed AABW during its transit between the deep ocean off Cape Darnley and 30°E. Cause (1) seems unlikely as shelf waters must reach the freezing point to undergo sea ice formation and dense water production.
 CDW warming at the continental slope off Cape Darnley could be caused by either a warming within the ACC [e.g., Gille, 2002] or by a southward migration of the ACC's Southern Boundary (SBdy) [Orsi et al., 1995] in response to changes in atmospheric forcing [Sallée et al., 2008]. To investigate the former hypothesis, the θ of the CDW core (defined as a mid-depth S maximum) is mapped onto dynamic height referenced to 1500 dbar for three periods (Figure 4b). The region closest to Cape Darnley with sufficient data coverage (80°E–90°E) was selected here. South of the SBdy (defined as a dynamic height of 0.51 ± 0.01 m referenced to 1500 dbar, black dashed lines) [Sokolov and Rintoul, 2009], no significant warming of the CDW in baroclinic streamfunction space is found (i.e., for a given dynamic height, the most recent θ is not systematically higher than for earlier periods), although the region's data paucity makes this difficult to state definitively.
 Instead, an indication of a southward SBdy translation is found in altimetric and hydrographic observations. Eastern Weddell gyre SSH (55°S–65°S, 30°E–90°E) exhibits a linear trend of 2.8 ± 0.6 mm yr−1 between 1996 and 2008; a total local sea level rise of 3.4 ± 0.48 cm over this period (Figure 4a). This suggests that the regional SBdy has migrated southward by around 100–200 km. Comparisons of the hydrographic SBdy positions in 1995 and 2006 (Figure 4a, red and light blue lines) with their altimetrically derived counterparts in 1996 and 2008 (white and black lines) reveal good agreement between the two techniques, supporting the use of altimetry to track the SBdy's movement. Given a climatological meridional gradient in the CDW core θ of ~0.2°C/100 km north of the Prydz Bay region (Figure 4b), the SBdy's observed southward translation implies a CDW core warming of 0.2°C–0.4°C near the continental slope. This compares favorably with the observed AABW warming of ~0.1°C, assuming a ~60% CDW component in the newly formed AABW [Foster and Carmack, 1976].
 A potentially pertinent feature of the regional circulation change between the mid-1990s and the late 2000s is the concurrent westward retreat of the Weddell gyre (Figure 4a), which may have facilitated the Indian sector-sourced AABW's penetration into the gyre's east. However, mean water mass ages calculated for the AABW CFC maximum using the TTD method [Waugh et al., 2004] with constant parameters (ventilated fraction CFC-12 saturation of 60%, Δ/−Γ = 1) indicate a greater-than-expected ageing (~25 years) between 1993 and 2008 (not shown), consistent with accompanying increases in apparent oxygen utilization. This is compatible with an increased rate of CDW entrainment.
 A possible issue with this explanation is that a southward SBdy shift should also increase the salinity of CDW entrained into the AABW layer. We estimate that the CDW salinity increase near the shelf break corresponding to a 0.2°C–0.4°C warming should be 0.01–0.03. This would accompany a 0.007–0.021 AABW salinity increase not observed at 30°E (Figure 3c). The reasons for this are unclear, yet a plausible conjecture is that the freshening of dense shelf waters upstream of the Amery region [e.g., Jacobs and Giulivi, 2010] may propagate westward by Antarctic slope flows and offset an increase in AABW salinity incurred by local entrainment of more saline CDW. A freshening trend of 0.003 year-1 since the late 1950s near the Ross Ice shelf has been linked to concurrent AABW freshening (by ~0.01 between 1993 and 2003/2004) as far west as ~85°E, immediately east of the Amery region [Jacobs and Giulivi, 2010].
 This study documents a decadal scale warming (by 0.1°C) and lightening (by 0.02–0.03 kg m−3) of the AABW entering the eastern Weddell gyre from the Indian sector, between the mid-1990s and late 2000s. These changes add to recent findings of decadal scale variations in AABW θ-S characteristics, which describe either freshening [Aoki et al., 2005; Rintoul, 2007; Jacobs and Giulivi, 2010] or warming linked to variable wind-forced bottom water export [Meredith et al., 2008, 2011; Jullion et al., 2010]. Our work attributes the observed AABW warming to a new mechanism: a change in the entrainment of warm, mid-depth waters into cascading shelf water plumes. This shifts the resultant bottom water mixture to a warmer and lighter class, consistent with the observed contraction of the coldest AABW [Purkey and Johnson, 2010, 2012]. This process most plausibly explains our measured AABW property changes and is concomitant with the poleward SBdy shift in the Prydz Bay region observed between 1996 and 2008. Insofar as the SBdy's southward migration off Cape Darnley is part of a recent, large-scale adjustment of the ACC to climatic changes in wind forcing [Sallée et al., 2008; Sokolov and Rintoul, 2009], we conjecture that the induction of AABW warming by changes in CDW entrainment may affect the formation area near the Adélie Land coast and wherever the ACC flows close to the Antarctic continental shelf. Fahrbach et al.  explain how wind-forced ACC translations affect the properties of CDW entering the Weddell gyre, which then influences the AABW formed. Therefore, such ACC shifts as the one we describe could also indirectly affect AABW produced in the Ross and Weddell gyres.
 We thank both reviewers for their helpful comments, the crews and science teams whose work has made this study possible, particularly Rana Fine, Sabrina Speich and Jim Happell for the I6S 2008 CFC data, NERC grant NE/E01366X/1 and NSF Grants OCE-0927583 and OCE-0622670 for financial support.
 The editor would like to acknowledge the work of two anonymous reviewers who contributed to the manuscript.