The Ross Sea Dipole – temperature, snow accumulation and sea ice variability in the Ross Sea region, Antarctica, over the past 2700 years
- 1Antarctic Research Centre, Victoria University of Wellington, Wellington, 6012, New Zealand
- 2GNS Science, Lower Hutt, 5010, New Zealand
- 3Department of Earth and Space Sciences, University of Washington, Seattle, WA 98195, USA
- 4Centre for Ice and Climate, Niels Bohr Institute, University of Copenhagen, Juliane Maries Vej 30, 2100 Copenhagen, Denmark
- 5College of Earth, Ocean, and Atmospheric Sciences, Oregon State University, Corvallis, OR 97330, USA
- 6Scripps Institution of Oceanography, UC San Diego, La Jolla, CA 92093, USA
- 7British Antarctic Survey, High Cross, Madingley Road, Cambridge, CB3 0ET, UK
- 8Physics and Astronomy, Curtin University, Perth, Western Australia, Australia
- 9Climate Change Institute, University of Maine, Orono, ME 04469-5790, USA
- 10Alfred Wegner Institute, Bremen, Germany
- 11Chinese Academy of Meteorological Sciences, Beijing, China
- 12State Key Laboratory of Cryospheric Science, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences, Lanzhou, Gansu, China
- 13DISAT, Department of Earth and Environmental Sciences, University Milano-Bicocca, Piazza della Scienza 1, 20126 Milano, Italy
- 14Department of Earth Sciences, Dartmouth College, 6105 Fairchild Hall, Hanover, NH 03755, USA
- 15Department of Chemical Engineering, SRM University, Kattankulathur 603203, Kancheepuram Dt., Tamil Nadu, India
- 16University of Tasmania, School of Biological Sciences, Hobart, TAS, 7001 Australia
- 17Specialty of Earth Sciences and Environment, UniLasalle, 19 rue Pierre Waguet, 60000 Beauvais, France
- 18Laboratoire des Sciences du Climat et de l'Environnement, LSCE/IPSL, CEA-CNRS-UVSQ, Université Paris-Saclay, 91198 Gif-sur-Yvette, France
- 19Institute for the Study of the Environment, Sustainability & Energy, Northern Illinois University, DeKalb, IL 60115, USA
- 20Geophysical Institute, University of Bergen, and Bjerknes Centre for Climate Research, 5020 Bergen, Norway
- 21Tianshan Glaciology Station, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences, Lanzhou, Gansu, China
- 22Department of Earth and Ocean Sciences, University of British Columbia, British Columbia, Canada
- 23State Key Laboratory of Earth Surface Processes and Resource Ecology, Beijing Normal University, Beijing, China
- 24Northwest Normal University, Lanzhou, Gansu, China
- anow at: University of Wisconsin-Madison, Department of Civil and Environmental Engineering, 660 N. Park St., Madison, USA
- bnow at: Faculty of Science and Engineering, University of Waikato, Hamilton, New Zealand
- cnow at: University of Rochester, Department of Earth & Environmental Sciences, Rochester, NY 14627, USA
- dnow at: Tonkin and Taylor, ABS Tower, 2 Hunter St., Wellington, 6011, New Zealand
- enow at: Center for Atmospheric Particle Studies, Carnegie Mellon University, Pittsburgh, PA 15213, USA
- fnow at: British Antarctic Survey, Cambridge, CB3 0ET, UK
Correspondence: Nancy A. N. Bertler (email@example.com)
High-resolution, well-dated climate archives provide an opportunity to investigate the dynamic interactions of climate patterns relevant for future projections. Here, we present data from a new, annually dated ice core record from the eastern Ross Sea, named the Roosevelt Island Climate Evolution (RICE) ice core. Comparison of this record with climate reanalysis data for the 1979–2012 interval shows that RICE reliably captures temperature and snow precipitation variability in the region. Trends over the past 2700 years in RICE are shown to be distinct from those in West Antarctica and the western Ross Sea captured by other ice cores. For most of this interval, the eastern Ross Sea was warming (or showing isotopic enrichment for other reasons), with increased snow accumulation and perhaps decreased sea ice concentration. However, West Antarctica cooled and the western Ross Sea showed no significant isotope temperature trend. This pattern here is referred to as the Ross Sea Dipole. Notably, during the Little Ice Age, West Antarctica and the western Ross Sea experienced colder than average temperatures, while the eastern Ross Sea underwent a period of warming or increased isotopic enrichment. From the 17th century onwards, this dipole relationship changed. All three regions show current warming, with snow accumulation declining in West Antarctica and the eastern Ross Sea but increasing in the western Ross Sea. We interpret this pattern as reflecting an increase in sea ice in the eastern Ross Sea with perhaps the establishment of a modern Roosevelt Island polynya as a local moisture source for RICE.
With carbon dioxide (CO2) and global temperatures predicted to continue to rise, model simulations of the Antarctic/Southern Ocean region show an increase in surface warming for the coming decades resulting in reduced sea ice extent, weakened Antarctic Bottom Water formation, intensified zonal winds that reduce CO2 uptake by the Southern Ocean, a slowing of the southern limb of the meridional overturning circulation (MOC) and associated changes in global heat transport, and a rapid ice sheet grounding line retreat that contributes to global sea level rise (Kusahara and Hasumi, 2013; Spence et al., 2012; Marshall and Speer, 2012; Sen Gupta et al., 2009; Toggweiler and Russell, 2008; Russell et al., 2006; Downes et al., 2010; Anderson et al., 2009; DeConto and Pollard, 2016; Joughin and Alley, 2011; Golledge et al., 2015; DeVries et al., 2017). Observations confirm an ozone-depletion-induced strengthening and poleward contraction of zonal winds (Thompson and Solomon, 2002b; Arblaster et al., 2011), increased upwelling of warm, modified Circumpolar Deep Water (Jacobs et al., 2011), a warmer Southern Ocean (Böning et al., 2008; Gille, 2002; Abraham et al., 2013), meltwater-driven freshening of the Ross Sea (Jacobs et al., 2002), ice shelf and mass loss, grounding line retreat (Rignot et al., 2014; Pollard et al., 2015; Paolo et al., 2015; Joughin et al., 2014), reduced formation of Antarctic Bottom Water (Rintoul, 2007) and Antarctic Intermediate Water (Wong et al., 1999), changes in sea ice (regional decreases and increases in the Amundsen and Ross seas, respectively) (Holland and Kwok, 2012; Sinclair et al., 2014; Stammerjohn et al., 2012), and dynamic changes in Southern Ocean CO2 uptake driven by atmospheric circulation (Landschützer et al., 2015). However, these observational time series are short (Böning et al., 2008; Gille, 2002; Toggweiler and Russell, 2008) and inter-model variability indicates that physical processes and their consequences are not well captured or understood (Braconnot et al., 2012; Sen Gupta et al., 2009). While the skill of equilibrium simulations steadily improves, the accuracy of transient model projections for the coming decades critically depends on an improved knowledge of climate variability, forcings and dynamic feedbacks (Stouffer et al., 2017; Bakker et al., 2017).
Here we present data from a new, highly resolved and accurately dated ice core record, spanning the past 2.7 kyr, from the eastern Ross Sea region. The Roosevelt Island Climate Evolution (RICE) ice core is compared with existing records in the region to investigate the characteristics and drivers of spatial and temporal climate variability in the Ross Sea region.
In this section, a brief overview is provided of the climatological and glaciological characteristics of the study site.
2.1 Dynamic interaction between tropical and midlatitudinal climate drivers and South Pacific climate variability
Environmental variability in the Pacific Sector of the Southern Ocean and Antarctica is dominated by three major atmospheric circulation patterns: the Southern Annular Mode (SAM), the El Niño–Southern Oscillation (ENSO) and the Inter-decadal Pacific Oscillation (IPO). The SAM is the leading empirical orthogonal function (EOF) of the Southern Hemisphere extratropical geopotential height fields on monthly and longer timescales and describes the strength and position of the Southern Hemisphere westerly winds via the relative pressure over Antarctica (∼ 65∘ S) and the midlatitudes (∼ 45∘ S) (Thompson and Wallace, 2000; Thompson and Solomon, 2002a). The persistent positive, summer trend of the SAM (decreasing pressure over Antarctica) has been linked to stratospheric ozone depletion and an increase in atmospheric greenhouse gas concentration (Arblaster et al., 2011; Thompson et al., 2011). The positive SAM is associated with above-average warming of the Antarctic Peninsula, cooler conditions over East Antarctica due to a reduced poleward pressure gradient and thus diminished transport of heat and moisture, and a reduction in katabatic flow (Marshall et al., 2013; Marshall and Thompson, 2016; Thompson and Solomon, 2002a). While the positive summer SAM trend (also weakly expressed during autumn) along the Antarctic margin is generally associated with an equatorward heat flux, the western Ross Sea is one of two regions (the Weddell Sea being the other) to experience an anomalous poleward heat flux (Marshall and Thompson, 2016) that transports heat and moisture across the Ross Ice Shelf. No such pattern is observed for regional surface air temperature (SAT) (Marshall and Thompson, 2016), which might be masked by the influence of regional sea ice variability on local temperatures. The positive SAM has been shown to contribute at least partially to an increase in total Antarctic sea ice, while a negative SAM has been associated with a reduced sea ice (Ferreira et al., 2015; Holland et al., 2017; Bintanja et al., 2013; Kohyama and Hartmann, 2015; Turner et al., 2017). The future behaviour of the SAM over the next decades is a topic of active research due to the competing and seasonally biased influences of projected stratospheric ozone recovery and greenhouse gas emissions (Bracegirdle et al., 2014; Gillett and Fyfe, 2013; Thompson et al., 2011).
The Pacific South American (PSA) patterns represent atmospheric Rossby wave trains initiated by anomalously deep tropical convection during ENSO events, in particular during austral spring, which originate in the western (PSA1) and the central (PSA2) tropical Pacific (Mo and Higgins, 1998). PSA1 and PSA2 are defined as the second and third EOF respectively of monthly-mean extratropical geopotential height fields, with the negative (positive) phase resembling El Niño (La Niña)-like conditions (Mo, 2000). Changes in SAT over West Antarctica have been linked to PSA1 variability (Schneider et al., 2012; Schneider and Steig, 2008), while the warming of West Antarctica's winter temperatures has been linked to PSA2 (Ding et al., 2011). The positive polarity of PSA1 is associated with anticyclonic wind anomalies in the South Pacific centred at ∼ 120∘ W, which have been linked to increased onshore flow and increased eddy activity (Marshall and Thompson, 2016). In contrast, during the positive phase of the PSA2, the anticyclonic centre shifts to ∼ 150∘ W in the Ross Sea, creating a dipole across the Ross Ice Shelf, with increased transport of marine air masses along the western Ross Ice Shelf and enhanced katabatic flow along the eastern Ross Ice Shelf (Marshall and Thompson, 2016). Sea ice feedbacks to the SAM and ENSO forcing in the western Ross Sea (as well as the Bellingshausen Sea) were found to be particularly strong when a negative SAM coincided with El Niño events (increased poleward heat flux, less sea ice) or a positive SAM concurred with La Niña events (decreased poleward heat flux, more sea ice) (Stammerjohn et al., 2008). The authors found that this teleconnection is less pronounced in the eastern Ross Sea.
The IPO, an ENSO-like climate variation on decadal timescales (Power et al., 1999), is closely related to the Pacific Decadal Oscillation (PDO) (Mantua and Hare, 2002). While the PDO is defined as the first EOF of sea surface temperature (SST) variability in the Northern Pacific, the IPO is defined by a tripole index of decadal-scale SST anomalies across the Pacific (Henley et al., 2015). A warm tropical Pacific and weakened trade winds are associated with a positive IPO, while a cooler tropical Pacific and strengthened trade winds are characteristic of a negative IPO. The phasing of the IPO and PDO have been shown to influence the strength of regional and global teleconnections with ENSO (Henley et al., 2015). An in-phase IPO amplification of ENSO events has been linked to a strengthening of global dry/wet anomalies, in contrast to periods when the IPO and ENSO are out of phase, causing these anomalies to weaken or disappear entirely (Wang et al., 2014). In addition, a negative IPO leads to cooler SSTs in the Ross, Amundsen and Bellingshausen seas, while a positive IPO is associated with warmer SSTs (Henley et al., 2015). The centre of anticyclonic circulation linked to precipitation at Roosevelt Island (Emanuelsson et al., 2018) moves eastward during the negative IPO from ∼ 120∘ W during the positive IPO to ∼ 100∘ W (Henley et al., 2015). It has been suggested that the negative IPO, at least in part, is responsible for the hiatus in global surface warming during 1940–1975 and 2001–2009 (England et al., 2014; Kosaka and Xie, 2013; Meehl et al., 2011).
The Amundsen Sea Low (ASL), a semi-permanent low-pressure centre in the Ross–Amundsen Sea, is the most prominent and persistent of three low-pressure centres around Antarctica, associated with the wave number 3 circulation (Raphael, 2004; Raphael et al., 2016; Turner et al., 2013). The ASL is sensitive to ENSO (especially during winter and spring) and SAM (in particular during autumn) and influences environmental conditions in the Ross, Amundsen and Bellingshausen seas and across West Antarctica and the Antarctic Peninsula (Ding and Steig, 2013; Raphael et al., 2016; Steig et al., 2012; Marshall and Thompson, 2016; Bertler et al., 2004; Turner et al., 2013; Thomas et al., 2009). Seasonally, the ASL centre moves from ∼ 110∘ W in during austral summer to ∼ 150∘ W in austral winter (Turner et al., 2013). A positive SAM and/or La Niña event leads to a deepening of the ASL, while a negative SAM and/or El Niño event causes a weakening (Turner et al., 2013). The IPO, through its effect upon ENSO and SAM variability, also influences the ASL and sea ice extent in the Ross and Amundsen seas (Meehl et al., 2016). Blocking events in the Amundsen Sea (Renwick, 2005) are sensitive to the position of the ASL and are dominant drivers of marine air mass intrusions and associated precipitation and temperature anomalies at Roosevelt Island (Emanuelsson et al., 2018).
2.2 RICE site characteristics
Roosevelt Island is an approximately 120 km long by 60 km wide grounded ice rise located near the north-eastern edge of the Ross Ice Shelf (Fig. 1). Ice accumulates locally on the ice rise, while the floating Ross Ice Shelf flows around Roosevelt Island. The ice surrounding Roosevelt Island originates from the West Antarctic Ice Sheet (WAIS), via the Bindschadler, MacAyeal and Echelmeyer ice streams. Bedmap2 data (Fretwell et al., 2013) suggest that the marine basins on either side of Roosevelt Island are roughly 600 m (western basin) and 750 m (eastern basin) deep and that the thickness of the Ross Ice Shelf at this location is about 500 m. At the RICE drill site (79.364∘ S, 161.706∘ W, 550 m above sea level) near the summit of Roosevelt Island, the ice is 764 m thick and grounded 214 m below sea level. Radar surveys across the Roosevelt Island ice divide show well-developed “Raymond arches” (Raymond, 1984) of isochrones suggesting a stable ice divide (Conway et al., 1999). The vertical velocity, constrained by phase-sensitive radio echo sounder (pRES) measurements, is approximately 20 cm a−1 at the surface relative to the velocity of 0 cm a−1 at the bed (Kingslake et al., 2014). A small migration of the divide has occurred in the past few centuries with the topographic divide off-set by about 500 m to the south-west. It is possible that the divide migrated as a result of an imbalance in the ice flux on either side of the divide, by either changes in the snow accumulation gradient or changes in the efflux across the grounding line due perhaps to changes in the buttressing by the Ross Ice Shelf. However, the negligible divide position migration magnitude suggests that neither snow accumulation gradient nor grounding line efflux have changed very much; this implies that the buttressing has not changed significantly either.
During two field seasons, 2011–2012 and 2012–2013, a 764 m long ice core to bedrock was extracted from the summit of Roosevelt Island. The drilling was conducted using the New Zealand intermediate depth ice core drill Te Wāmua Hukapapa (“Ice Cores That Discover the Past” in NZ Te Reo native language). The drill system is based on the Danish Hans Tausen Drill with some design modification (Mandeno et al., 2013). The upper 60 m of the borehole was cased with plastic pipe and the remainder of the drill hole filled with a mixture of Estisol-240 and Coasol to prevent closure. The part of the RICE ice core record used in this study covers the past 2.7 kyr and consists of data combined from the RICE-2012/13-B firn core (0.19–12.30 m depth) and the RICE Deep ice core (12.30–344 m depth). In addition, the uppermost samples from a 1.5 m deep snow pit were used to extend the firn and ice core record for the month of December 2012. An overview of the core quality and processing procedures are summarised by Pyne et al. (2018). Here, we present new water stable-isotope (deuterium, δD) and snow accumulation records and compare them with existing records from West and East Antarctica (Table 1).
3.1 RICE age model: RICE17
The RICE17 age model for the past 2.7 kyr is based on an annually dated ice core chronology from 0 to 344 m which is described in detail by Winstrup et al. (2017). The cumulated age uncertainty for the past 100 years is years, for the past 1000 years years and for the past 2000 years years, reaching a maximum uncertainty of ±45 years at 344 m depth (2.7 kyr). The RICE17 timescale is in good agreement with the WD2014 annual-layer counted timescale from the WAIS Divide ice core dating to 200 CE (280 m depth). For the deeper parts of the core, there is likely a small bias (2–3 %) towards undercounting the annual layers, resulting in a small age offset compared to the WD2014 timescale.
3.2 Snow accumulation reconstruction
Ice core annual layer thicknesses provide a record of past snow accumulation once the amount of vertical strain has been accounted for. At Roosevelt Island, repeat pRES measurements were performed across the divide, providing a direct measurement of the vertical velocity profile (Kingslake et al., 2014). This has a key advantage over most previous ice core inferences of accumulation rate because vertical strain thinning through the ice sheet is measured directly, rather than needing to use an approximation for ice flow near ice divides (e.g. Dansgaard and Johnsen, 1969; Lliboutry, 1979). Uncertainty in the accumulation-rate reconstruction increases from zero at the surface (no strain thinning) to ±10 % at 78 m true depth (1712 CE). Below 78 m, the uncertainty remains constant at ±10 %. A detailed description of the accumulation-rate reconstruction is provided by Winstrup et al. (2017).
3.3 Water stable-isotope data
The water stable-isotope record was measured using a continuous-flow laser spectroscopy system with an off-axis integrated cavity output spectroscopy (OA-ICOS) analyser, manufactured by Los Gatos Research (LGR). The water for these measurements was derived from the inner section of the continuous flow analysis (CFA) melt head, while water from the outside section was collected for discrete samples. A detailed description and quality assessment of this system is provided by Emanuelsson et al. (2015). The combined uncertainty for deuterium (δD) at 2 cm resolution is ±0.85 ‰. A detailed description of the isotope calibration, the calculation of cumulative uncertainties, and the assignment of depth is provided by Keller et al. (2018).
The ERA-Interim (ERAi) reanalysis data set of the European Centre for Medium-Range Weather Forecasts (ECMWF; Dee et al., 2011), along with firn and ice cores, snow stakes and an automatic weather station (AWS) are used to characterise the meteorology of Roosevelt Island. ERAi data have been extracted for the RICE drill site from the nearest grid point (S 79.50 ∘, W 162.00 ∘; Fig. 1b) for the common time period between 1979 and 2012. The year 1979, the onset of the ERAi reanalysis, occurs at 13.42 m depth in the firn. For this reason, the period 1979–2012 is predominantly captured in the RICE 12/13 B firn core. Data from the RICE AWS suggest that precipitation at RICE can be irregular, with large snow precipitation events dominating the accumulation pattern (Emanuelsson, 2016). Therefore, we limit the analysis in this study to annual averages and longer-term trends.
4.1 Isotope temperature correlation
The borehole temperature measured in 2012 in two 11 and 12 m deep drill holes suggest an average annual temperature of −23.5 ∘C. This stands in stark contrast to the average annual temperature derived from ERAi data of −27.4 ∘C at the RICE site. Furthermore, the RICE AWS also recorded an average annual temperature of −23.5 ∘C. In contrast, the nearby Margaret AWS (located at 67 m a.s.l., just 96 km south-west of the RICE AWS; data obtained from Antarctic Meteorological Research Center and Automatic Weather Station Project; https://amrc.ssec.wisc.edu) records an average annual temperature of −26.6 ∘C. While recorded summer temperatures at RICE and Margaret AWS agree well, during winter the Margaret AWS records up to 10–15 ∘C colder 3-hourly temperatures than the RICE AWS. It is possible that rime build-up at the RICE AWS during winter (Supplement Fig. S1) might have provided insulation that allowed for residual heat from the sensors to warm the temperature cavity leading to erroneously warm readings. Alternatively, it is possible that the Margaret AWS site is influenced by stronger temperature inversions leading to exceptionally cold temperatures of −60 ∘C, while the topography of Roosevelt Island might be less conducive to such conditions. A comparison between high-resolution borehole temperature measurements conducted at RICE from November 2013 to November 2014 and AWS data, including snow temperature measurements, will provide important insights into this temperature off-set. Until this analysis is concluded, we argue that ERAi data, which agree well with the Margaret AWS observations, provide the most reliable temperature time series to calibrate the stable-isotope–temperature relationship.
In Fig. 2a, the ERAi SAT time series extracted for the RICE drill site is compared with the ERAi SAT spatial grid. The analysis suggests that temperature variability at RICE is representative of variability across the Ross Ice Shelf (with the exception of the westernmost margin along the Transantarctic Mountains), northern Victoria Land, western Marie Byrd Land, and the Ross and Amundsen seas. Furthermore, the Antarctic Dipole pattern (Yuan and Martinson, 2001), a negative correlation between the SAT in the Ross–Amundsen Sea region and that of the Weddell Sea, is also captured in the data. The locations of the Siple Dome, West Antarctic Ice Sheet Divide ice core (WDC), Talos Dome, TALDICE and Taylor Dome ice cores fall within the region of positive RICE SAT correlation.
The correlation between RICE δD data and ERAi SAT (Fig. 2b) remains positive across the Ross Ice Shelf and northern Ross Sea, but the WDC site now falls outside the field of the statistically significant correlation. The time series correlation between the ERAi SAT record and the RICE δD data (Fig. 2d) is r=0.42(p<0.01). We test the robustness of this relationship by applying the minimum and maximum age solutions within the age uncertainty (≤2 year during this time period; Winstrup et al., 2017) to identify the age model solution within the age uncertainty that renders the highest correlation. This optimised solution RICE δDo is shown in Fig. 2e with a correlation coefficient of r=0.66(p<0.001). The correlation of the RICE δDo record with the ERAi SAT data (Fig. 2c) produces a pattern that more closely resembles the correlation pattern using the ERAi data itself (Fig. 2a), suggesting that the δD record provides useful information about the regional temperature history.
From the comparison between RICE δDo and ERAi SAT records, we obtain a temporal slope of 3.37 ‰ ∘C−1 (Fig. 2f), which falls within the limit of previously reported values from Antarctica of ∼ 2.90–3.43 ‰ ∘C−1 for temporal (interannual) slopes (Schneider et al., 2005) and ∼ 6.80±0.57 ‰ ∘C−1 for spatial slopes (Masson-Delmotte et al., 2008). We use this relationship to calculate temperature variations for the RICE δD record. The average annual temperature calculated for 1979–2012 from ERAi for the RICE site is ∘C and ∘C for the δDo data. Although the year-to-year SAT variability appears to be well captured in the RICE δDo record, there are discrepancies in observed trends. While RICE δDo data suggest an increase in SAT from 1996 onwards, ERAi SAT data do not show a trend (Fig. 2e). It remains a challenge to determine how well reanalysis products, including ERAi data, and other observations, including isotope data, capture temperature trends in Antarctica (PAGES2k Consortium, 2013; Stenni et al., 2017) and thus whether the observed difference in the trend between ice core δDo and ERAi SAT is significant or meaningful. We also compare the δDo with records from AWS (Ferrell, Gill and Margaret AWS) and stations (Byrd, McMurdo, Scott Base, Siple Stations) in the region (Fig. S2 and Table S1, Supplement). The comparison is hampered by the shortness of the records and gaps in the observations. Only years were used for which monthly values were reported for each month of the year. No statistically significant correlation was identified between δDo and available data.
Furthermore, we test the correlation with the near-surface Antarctic temperature reconstruction by Nicolas and Bromwich (2014; referred to as NB2014), which uses three reanalysis products and takes advantage of the revised Byrd Station temperature record (Bromwich et al., 2013) to provide an improved reanalysis product for Antarctica for the time period 1958–2012 CE. We find no correlation between the NB2014 record and the ERAi data at the RICE site, nor the RICE δDo data for the 1979–2012 time period, perhaps suggesting some regional challenges. If the full time period available for the NB2014 data is considered (1957–2012), the NB2014–RICE δDo correlation becomes weakly statistically significant with r=0.23 (p=0.09, Table S1).
4.2 Regional snow accumulation variability
Temporal and spatial variability in snow accumulation are assessed using 144 snow stakes covering a 200 km2 array. The 3 m long, stainless steel poles were set and surveyed in November 2010, re-measured in January 2011, and revisited and extended in January 2012 and November 2013. The measurements indicate a strong accumulation gradient with up to 32 cm water equivalent per year (w.e. a−1) on the north-eastern flank decreasing to 9 cm w.e. a−1 on the south-western flank. Near the drill site, annual average snow accumulation rates range from 22±4 cm w.e. a−1 from 2010 to 2013.
In addition, snow accumulation was measured using an ultrasonic sensor mounted on the RICE AWS. The sensor was positioned 140–160 cm above the ground and reset during each season. The 3-year record shows gaps (Fig. 3) which represent times when rime on the sensor and/or blowing snow caused erroneous measurements. This condition was particularly prevalent during winter. Over the 3 years, the site received an average snowfall of ∼ 75 cm a−1. Assuming an average density of 0.37 g cm−3 (average density from two snow pits, 0–75 cm), the AWS data suggest ∼ 20 cm w.e. a−1 accumulation, which is comparable with the accumulation rate derived from the ice core (21±6 cm w.e. a−1 for the period 1979–2012; Winstrup et al., 2017). In contrast, ERAi data suggest an average annual snow accumulation of only 11 cm w.e. a−1. It has been shown that Antarctic ERAi data capture precipitation variability but generally underestimate the precipitation total (Wang et al., 2016; Sinclair et al., 2010; Bromwich et al., 2011). Further, the ERAi data are not directly comparable to local measurements because they do not capture periods of snow scouring by wind. Yet, there is a good agreement between the two data sets with respect to the timing and relative rate of precipitation, which suggests that neither winters nor summers have been times of significant snow scouring. We attribute the difference between the ERAi data and our measurements to the spatial differences between measurements of the snow stake array, the interpolation field of the nearest ERAi data point and the actual drill site location, as well as differences in assumed snow densities or different methodologies in the conversion from precipitation to water-equivalent units. The regional representativeness of RICE snow accumulation data is assessed by correlating the ERAi precipitation time series, extracted for the RICE location, with the ERAi precipitation grid data (Fig. 4a). The correlation suggests that precipitation variability at Roosevelt Island is representative of the observed variability across the Ross Ice Shelf, the southern Ross Sea, and western West Antarctica. We note from Fig. 4a that the sites of the Siple Dome ice core (green circle) and the WDC (red circle) are situated within the positive correlation field, while Talos Dome (purple circle) and Taylor Dome (orange circle) show no correlation to ERAi precipitation at RICE. A negative correlation is found with the region of the South Pacific, Antarctic Peninsula and eastern West Antarctica. In Fig. 4b, the RICE snow accumulation record is correlated with ERAi precipitation data and shows a similar pattern. The resemblance of the correlation patterns suggests that the variability in the RICE snow accumulation data (Fig. 4b) reflects regional precipitation variability (Fig. 4a) and thus can likely elucidate regional snow accumulation variability in the past, in particular for array reconstructions such as Thomas et al. (2017). We also test the correlation with the optimised age scale derived for the δDo record and find that for snow accumulation data this adjusted age scale (Acco) reduces the correlation but remains statistically significant (Table 2). This result suggests that the optimised age solution is not superior to the RICE17 age scale, and we note that the sensitivity of the correlation to those minor adjustments is founded in the brevity of the common time period. However, there is no significant difference between the overall pattern and relationships of the two age scale solutions.
4.3 Influence of regional sea ice variability on RICE isotope and snow accumulation
Sea ice variability has been shown to influence isotope values in precipitated snow, particularly in coastal locations (Küttel et al., 2012; Noone and Simmonds, 2004; Thomas and Bracegirdle, 2009) through the increased contribution of enriched water vapour during times of reduced sea ice and increased sensible heat flux due to a higher degree of atmospheric stratification leading to more vigorous moisture transport. Tuohy et al. (2015) demonstrated that for the period 2006–2012, ∼ 40–60 % of precipitation arriving at Roosevelt Island came from local sources in the southern Ross Sea. In addition, Emanuelsson et al. (2018) demonstrated the important role of blocking events that are associated with over 88 % of large precipitation events at RICE, on sea ice variability via meridional wind field anomalies.
Snow accumulation at RICE is negatively correlated with sea ice concentration (SIC) in the Ross Sea region and northern Amundsen Sea region (Fig. 5a), which predominately represents sea ice exported from the Ross Sea. We observe years of increased (decreased) SIC leading to reduced (increased) accumulation at RICE, confirming the sensitivity of moisture-bearing marine air mass intrusions to local ocean moisture sources and hence regional SIC. The correlation between ERAi SIC and the optimised RICE δDo record (Fig. 5b) similarly shows a negative correlation of SIC in the Ross Sea (perhaps with the exception of the Ross and Terra Nova polynyas) and the northern Amundsen Sea, suggesting more depleted (enriched) values during years of increased (reduced) SIC.
In Fig. 5c and d, the sea ice extent index (SIEJ) for the Ross–Amundsen Sea, developed by Jones et al. (2016), is correlated with ERAi SAT and precipitation data. The analysis also identifies the co-variance of sea ice extent (SIE) and SAT, with increasing (decreasing) sea ice coinciding with cooler (warmer) SAT. This suggests that during years of increased SIE, the Ross Ice Shelf and western Marie Byrd Land experience lower temperatures and less snow accumulation. The correlation between SIEJ and ERAi precipitation at RICE is , and for SIEJ and RICE snow accumulation it is (Table 2). Moreover, the correlation between SIEJ and ERAi SAT and SIEJ and RICE δDo is also statistically significant with and , respectively. The higher correlation with RICE δDo perhaps suggests that the influence of SIE in the Ross Sea region affects the RICE δD record both through direct temperature changes in the region as well as fractionation processes that are independent of temperature, such as the lengthened distillation pathway to RICE during periods of more extensive SIE.
The ERAi SAT and ERAi precipitation data at RICE (Table 2) reveal a positive correlation over large areas of Antarctica with higher correlation coefficients over the eastern Ross Sea and eastern Weddell Sea (spatial fields not shown). At the RICE site, the correlation reaches r=0.66 (p<0.001). Moreover, the correlation between RICE δD and RICE snow accumulation data (RICE Acc) (or RICE δDo and RICE Acco) data is statistically significant, with r=0.49 (p<0.01) (or ro=0.62, po<0.001. This suggests that years with positive isotope anomalies are frequently characterised by higher snow accumulation rates. In contrast, precipitation during low snow accumulation years might be dominated by precipitation from air masses that have travelled further and perhaps across West Antarctica (Emanuelsson et al., 2018) leading to more depleted isotope values and lower snow accumulation rates than local air masses from the Ross Sea region.
4.4 Influence of climate drivers on prevailing conditions in the Ross Sea region
Seasonal biases and the enhancing or compensating effects of the relative phasing of SAM, ENSO and IPO conditions, on seasonal, annual and decadal timescales make linear associations of climate conditions and their relationship with climate drivers in the South Pacific challenging. We use the Southern Annular Mode Index (SAMA) developed by Abram et al. (2014) to test the fidelity of the SAM relationship with the climatic conditions in the Ross Sea over the past millennium (Table 2). The SAMA is highly correlated (r=0.75) with the SAM record developed by Marshall (2003) for their common time period (1957–2009). In addition, the Southern Oscillation Index (SOI; Trenberth and Stepaniak, 2001), Niño 3.4 Index (Rayner et al., 2003b), Niño 4 Index (Trenberth and Stepaniak, 2001) and the IPO Index (Henley et al., 2015) are used to investigate the influence of SST variability in the eastern and central tropical Pacific on annual and decadal timescales (IPO). In addition, we take advantage of an 850-year reconstruction of the Niño 3.4 index (Emile-Geay et al., 2013) to investigate any long-term influence of the eastern Pacific SST on environmental conditions in the Ross Sea.
The correlation of ERAi data and modern ice core records covering the 1979–2012 CE period with indices of relevant climate drivers (Table 2) suggests that SAMA has an enduring statistically significant relationship with temperature, snow accumulation and SIE in the Ross Sea, with the positive SAM being associated with cooler temperatures, lower snow accumulation or precipitation and more extensive SIE. The correlations remain robust and at comparable levels using a detrended SAMA record. In contrast, ENSO (SOI, Niño 3.4 and 4) and ENSO-like variability (IPO) have only linear statistically significant relationships with ERAi precipitation (but not with RICE snow accumulation) and SIEJ. The dynamic relationship between the phasing of SAM, ENSO and IPO maybe masking aspects of the interactions (Fogt and Bromwich, 2006; Marshall and Thompson, 2016). In 2010, an anomalously cold year is observed. If only the time series from 1979 to 2009 is considered, the correlations between RICE δD and these considered climate drivers becomes statistically significant: SOI (, p=0.006), Niño 3.4 (r=0.48, p=0.007), Niño 4 (r=0.57, p=0.001) and IPO (r=0.44, p=0.014). This further highlights the vulnerability of this analysis to individual years due to the brevity of the time series further complicating a linear analysis between individual drivers and regional responses. Moreover, statistically significant correlations might also be obtained if seasonal averages could be used for the comparison as ENSO events usually peak during the austral summer, in particular December (Turner, 2004). Nonetheless, this analysis confirms previous findings that the Ross Sea region is sensitive to the cumulative, independent and dependent influences of SAM, ENSO and the IPO.
Decadally smoothed RICE isotope and snow accumulation records for the past 2.7 kyr (Fig. 6) are compared with published data from the Ross Sea region (Siple Dome – green), coastal East Antarctica (Talos Dome/TALDICE – purple; Taylor Dome – orange) and West Antarctica (WDC – red).
5.1 Regional temperature variability
We find that the RICE and Siple Dome (Brook et al., 2005) water isotope records share a long-term isotopic warming trend in the Ross Sea region. In contrast, WDC isotope (Steig et al., 2013) and borehole temperature data (Orsi et al., 2012) exhibit a long-term cooling trend for West Antarctica, while TALDICE (Stenni et al., 2002) and Taylor Dome (Steig et al., 1998, 2000) recorded stable-isotopic conditions for coastal East Antarctica in the western Ross Sea.
Elevation changes influence water isotope values (Vinther et al., 2009). The thinning of Roosevelt Island, inferred from the amplitude of arched isochrones beneath the crest of the divide and the depth–age relationship from the ice core (Conway et al., 1999), is less than 2 cm a−1 for the past 3.5 kyr. Thus, the surface elevation has decreased less than 50 m over the past 2.7 kyr. Assuming that these elevation changes are sufficient to influence vertical movement of the precipitating air mass, such an elevation change could account for an isotopic enrichment of δD = ∼ 2 ‰ (Vinther et al., 2009), which is insufficient to explain the total observed increase of 8 ‰. Furthermore, the RICE δD trend is characterised by two step changes at 580 CE ± 27 years and 1477 CE ± 10 years (grey dotted lines in Fig. 6). These change points were identified using a minimum threshold parameterisation to achieve a minimised residual error (Killick et al., 2012; Lavielle, 2005). At the identified change points, the decadal isotope values increase by ∼ 3 and ∼ 5 ‰, respectively, which suggests that elevation changes were not a principal driver. Using the temporal slope of 3.37 ‰ per degree ∘C, these abrupt temperature transitions could represent an increase in the average decadal temperature (Fig. 7a) from −28.5 to −27.7 ∘C and from −27.7 to −26.2 ∘C. An underlying influence from long-term thinning, accounting for a δD shift of 2.4 ‰, would exaggerate the observed warming of 2.3 ∘C by 0.7 ∘C, thus suggesting a minimum isotopic temperature warming of at least 1.6 ∘C. The modern decadal isotope temperature average (2003–2012) of −25.1 ∘C (pink bar, Fig. 7a) and ERAi temperature of −26.5 ∘C lie within the 1σ distribution of the natural decadal temperature variability in the past 500 years. We note that changes in atmospheric circulation and sea ice extent might also have contributed significantly to the change in the observed isotopic shift, and we offer some suggestions in the following sections.
The Siple Dome ice core δ18O record exhibits a similar isotope history to the RICE δD record. Siple Dome isotope data reveal an abrupt warming or isotopic enrichment at 605 CE, some 25 years later than in RICE but within the cumulative age uncertainty of the two records. After 605 CE, Siple Dome isotope temperatures remain stable, although recording somewhat warmer isotope temperatures from about 1875 CE. Late-Holocene elevation changes (thinning) at Siple Dome have been reported to be negligible (Price et al., 2007) and are unlikely to have caused the observed abrupt isotopic shift at 605 CE. In contrast to records from the western Ross Sea (Bertler et al., 2011; Rhodes et al., 2012; Stenni et al., 2002) and West Antarctica (Orsi et al., 2012), RICE and Siple Dome do not show an isotopic warming or cooling associated with the Medieval Warm Period (MWP) or the Little Ice Age (LIA), respectively.
The WDC δ18O record suggests a long-term isotope cooling of West Antarctica, confirmed by borehole temperature reconstructions (Orsi et al., 2012). This trend is consistent with warmer than average temperatures during the MWP and cooler conditions during the LIA but may also reflect changes in elevation and decreasing insolation (Steig et al., 2013). The cooling trend is followed by an increase in temperature in recent decades (Orsi et al., 2012; Steig et al., 2009) consistent with an increase in marine air mass intrusions (Steig et al., 2013). We note that within 200 years of the onset of the isotopic warming at RICE (at 580 CE ± 27 years), the WDC borehole temperature and isotope data start to record a temperature decline, in line with the observed anti-phased relationship of WDC with RICE and Siple Dome. No notable change is observed in WDC water stable-isotope temperature data in the late 15th century. In contrast, WDC borehole temperature suggests the onset of a warming trend within the last 100 years, marking the modern divergence between WDC isotope and borehole records. The TALDICE and Taylor Dome water stable-isotope temperatures do not exhibit a long-term trend over the past 2.7 kyr. Yet colder water stable-isotope temperature anomalies have been associated with the LIA period at both sites (Stenni et al., 2002), which coincide with cooler conditions at WDC and the intensified increase in isotope temperature at RICE.
The similarity between the RICE and Siple Dome isotope records suggests that the eastern Ross Sea was dominated by regionally coherent climate drivers over the past 2.7 kyr, perhaps receiving precipitation via similar air mass trajectories. Overall this comparison shows that isotope temperature trends in the eastern Ross Sea (isotopic warming at RICE and Siple Dome) and West Antarctica (WDC cooling) were anti-phased for over 2 kyr (660 BCE to ∼ 1500 CE), while the western Ross Sea (TALDICE) remained stable, forming a distinct Ross Sea Dipole pattern. From the 17th century onwards this relationship changes. While WDC water stable-isotope temperatures continue to cool, from the 17th century, the WDC borehole temperature records a warming. At the same time, RICE and Siple Dome experience warmer isotope temperatures while TALDICE recovers from its coldest recorded isotope temperature during the study period.
5.2 Regional snow accumulation variability
Investigating long-term trends in snow accumulation records (Fig. 6b), the decadally smoothed RICE shows a discernible positive trend from about 600 CE of about 0.2±0.1 cm w.e. per century (Winstrup et al., 2017) for the eastern Ross Sea, while WDC (Fudge et al., 2016) displays a decreasing trend for central West Antarctica. The RICE snow accumulation data reach a maximum in the 13th century, with a trend towards lower values from the late 17th century onwards of about cm w.e. per century (Winstrup et al., 2017). Since 1950 CE, this trend has steepened to -6.6 cm w.e. per century (Winstrup et al., 2017). Based on the negative correlation between RICE snow accumulation and SIC in recent decades, we interpret the long-term increase in snow accumulation as representing a long-term reduction in SIC in the Ross Sea, consistent with a long-term increase in RICE isotope temperature. The recent rapid decline in snow accumulation rates could be related to increases in sea ice conditions in the eastern Ross Sea, perhaps marking the modern onset of local sea ice expansion. The modern decadal average (2002–2012) of 20 cm w.e. a−1 lies within the 2σ variability in decadal RICE ice core snow accumulation rates (Fig. 7). Talos Dome records its maximum snow accumulation rates at the end of the 13th century and reduced snow accumulation during the Little Ice Age (Stenni et al., 2002). Until the 15th century, RICE and WDC snow accumulation and isotope data show an expected positive correlation between their respective isotope and snow accumulation records. Regionally, RICE and WDC isotope and snow accumulation are anti-phased. From the 16th century onwards, this relationship reverses and RICE and WDC snow accumulation are now in phase, suggesting below-average snow accumulation in the eastern Ross Sea and West Antarctica. We note that from the 16th century onwards, snow accumulation at RICE and WDC displays a negative correlation with water stable isotope (RICE) and borehole temperature (WDC) reconstructions. At RICE this relationship is again positive for 1979–2012. During the 20th century, Talos Dome records an increase in snow accumulation of ∼ 11% in the western Ross Sea (Stenni et al., 2002), in contrast to the observed snow accumulation decrease at RICE and WDC. However, the values are not unique within the variability in the 800 years captured in the Talos Dome record.
Palaeo-reconstructions of the SAMA (Abram et al., 2014) and Niño 3.4 (Emile-Geay et al., 2013) indices (Fig. 6) provide important opportunities to investigate the influence of dominant drivers of regional climate conditions over the past millennium. In particular, the Niño 3.4 index captures the ENSO signal originating in the central-eastern tropical Pacific associated with the PSA1 pattern. Emile-Geay et al. (2013) note that while the reconstructions based on three model outputs agree well on decadal to multi-decadal time periods, they show different sensitivities at centennial resolution (but not different signs). The SAM index (Thompson and Wallace, 2000; Thompson and Solomon, 2002a) was developed during the late 20th century, at a time when SAM was characterised by a strong positive trend. The SAMA reconstruction showed that the modern SAM is now at its most positive state in all of the past millennium (Abram et al., 2014). As a consequence, the reconstructed SAMA is mainly negative. To investigate the influence of positive and negative anomalies of the SAMA relative to its average state over the past 1 kyr, we plot the SAMA reconstruction by indicating values as being above (light purple) or below (purple) the long-term average of −1.3 rather than 0. The traditional positive SAMA values (above 0, dark purple) are also shown for reference. Assessing the relationship between RICE, Siple Dome, WDC and TALDICE, we identify three major time periods of change: 660 BCE to 1367 CE (long-term baseline), 1368 to 1683 CE (negative SAMA) and 1684 to 2012 CE (onset of the positive SAMA).
6.1 Long-term baseline 660 BCE to 1367 CE
We find that for over 2 kyr – from 660±44 BCE to 1367 ±12 CE – the eastern Ross Sea (RICE and Siple Dome) shows an enduring anti-phase relationship with West Antarctica (WDC), while coastal East Antarctica in the western Ross Sea (TALDICE, Taylor Dome) remains neutral (Fig. 6). Moreover, with some minor exceptions, isotope and snow accumulation records at RICE, WDC and TALDICE are positively correlated.
6.2 Negative SAMA – 1368 to 1683 CE
The SAMA reconstruction suggests that, over the past millennium, the SAM was at its most negative (Abram et al., 2014) from 1368±12 years CE to 1683±8 CE years. As noted by Abram et al. (2014), the SAMA and Niño 3.4 reconstructions (Emile-Geay et al., 2013) are anti-phased on multi-decadal to centennial timescales with the Niño 3.4 index recording some of the warmest SSTs over the past 850 years during this period of negative SAMA.
During the negative SAMA, RICE shows a distinct and sudden increase in isotope temperature, while TALDICE records its coldest conditions over the past 2.7 kyr. The Taylor Dome record also shows prolonged cold isotope temperature anomalies during this time period. Previously published shorter records from the western Ross Sea from Victoria Lower Glacier in the McMurdo Dry Valleys (Bertler et al., 2011) and Mt Erebus Saddle (Rhodes et al., 2012) also suggest colder conditions in the western Ross Sea during this period, with more extensive sea ice and stronger katabatic flow. We observe that WDC and TALDICE show below-average snow accumulation values, while RICE snow accumulation changes from a long-term positive to a negative trend. Such trends are consistent with the reported increased SIE in the western Ross Sea (colder SAT and lower snow accumulation at TALDICE; cooler conditions with more extensive sea ice and stronger katabatic winds at Victoria Lower Glacier and Mt Erebus) and Bellingshausen Sea (less snow accumulation and colder SAT at WDC). In contrast, RICE records warmer isotope temperatures along with less and more variable snow accumulation, displaying a distinct Ross Sea Dipole. Coinciding with the sudden increase in RICE δD in 1492 CE is the decoupling of the local isotope temperature from snow accumulation, evident from the diversion of the RICE snow accumulation and δD trends. The reduction in snow accumulation might be linked to a negative SAM-induced weakening of the ASL, perhaps leading to the development of fewer blocking events in the eastern Ross Sea. Alternatively, the abrupt change to warmer isotope temperatures at RICE might also point towards the development of the Roosevelt Island polynya. In recent decades, a Roosevelt Island polynya has been observed and merges at times with the much larger Ross Sea polynya (Morales Maqueda et al., 2004). In contrast to the Ross Sea Polynya (Sinclair et al., 2010), a local polynya could provide a potent source of isotopically enriched vapour for precipitation at RICE, perhaps exaggerating the actual warming of the area as interpreted from water stable-isotope data. We expect the influence of a Roosevelt Island polynya to have a reduced effect on the more distant Siple Dome, which is consistent with our observations.
6.3 Onset of the positive SAM – 1684 to 2012 CE
At 1684 CE ±7 years, the SAMA increases and remains above its long-term average until modern times while the Niño 3.4 index suggests a change to the prevalence of strong La Niña-like conditions, conditions conducive to a strengthening of the ASL. RICE δD suggest the continuation of warm, isotopically enriched conditions, while snow accumulation drops below the long-term average, with the RICE snow accumulation trend now in phase with the negative trend at WDC (Fig. 6). At the same time, Talos Dome records highly variable snow accumulation rates with an 11 % increase in snow accumulation rates from the 20th century onwards. The change to above-average SAMA (or even positive SAMA) values coincides with the onset of the diversion of WDC water isotope and borehole temperature reconstructions and the decoupling of the RICE δD and snow accumulation trends. Coincident positive SAM (purple SAMA values in Fig. 6c) and La Niña events have been linked in recent decades to increases in SIE in the western Ross Sea and decreases in the Bellingshausen Sea (Stammerjohn et al., 2008). This is consistent with the notable reduction in snow accumulation at RICE and the trend towards warmer conditions and increased marine air mass intrusions into West Antarctica as inferred from WDC isotope data (Steig et al., 2013) but is inconsistent with the reduction in snow precipitation at WDC and the trend to warmer isotope temperatures at RICE. We interpret the continuation of warm RICE isotope temperatures to reflect the persistence of the Roosevelt Island polynya.
6.4 Dipole pattern on decadal to centennial timescales
To investigate the drivers of decadal to centennial variability, we compare the linearly detrended time series of RICE water stable-isotope records with those from (i) Siple Dome and WDC (West Antarctica; Fig. 8a) and (ii) TALDICE (East Antarctica, western Ross Sea; Fig. 8b). The analysis suggests that from about 500 CE onwards, RICE and Siple Dome variability are in phase with West Antarctic climate variability (WDC). In contrast, RICE and TALDICE isotope variability alternates between spatial pattern of in-phase (purple) and anti-phase (grey, Ross Sea Dipole) relationships. During the negative phase of the SAMA (Fig. 8), the anti-correlation between RICE and TALDICE is particularly strong.
To assess the correlation of cyclicities apparent in the RICE, Siple Dome, WDC and TALDICE isotope records, wavelet coherence spectrum analyses were conducted (Fig. 9) on the time series shown in Fig. 8. The analysis of RICE and Siple Dome (Fig. 9a) suggests that the two records positively correlate on a broad spectrum of frequencies with cyclicities between 200 and 500 years. The correlation is weakest during 660–100 BCE. A strong anti-phased coherence is also observed for the 30–70-year periodicity from 100 to 800 CE. The high coherency suggests that RICE and Siple Dome respond to similar forcings. The coherence analysis between RICE and WDC shows an enduring in-phase correlation from ∼ 1000 CE to today for the bandwidth of 200–700 years. An anti-phase coherence is found from 0 to 500 CE. The coherence analysis between RICE and TALDICE identifies strong relationships predominantly for the early part of the records, from 660 BCE to ∼ 800 CE, and a weak coherence from about 800 to 1700 CE, when RICE leads by ∼ 75–100 years. The analysis suggests that for the past 2.7 kyr the eastern Ross Sea (RICE, Siple Dome) and western West Antarctica (WDC) are climatologically closely linked in their response to forcings on decadal to centennial timescales and are positively correlated for the past 1.6 kyr. In contrast, the relationship between the western (TALDICE) and eastern (RICE, Siple Dome) Ross Sea is more variable.
The recent change to a strongly negative SAM (Marshall Index −3.12) in November 2016 coincided with a significant reduction in Antarctic SIE, including the Ross Sea, during the 2016/17 summer (Turner et al., 2017). Longer observations are necessary to assess whether this recent trend continues and indeed forces the reduced SIE, but it fuels questions on the potential acceleration of future environmental change in the Antarctic/Southern Ocean region. To improve projections for the coming decades, an improved understanding of the interplay of teleconnections and local feedbacks is needed.
The Ross Sea region is a climatologically sensitive region that is exposed to tropical and midlatitude climate drivers. The ASL has been shown to deepen during coinciding positive SAM and La Niña events and to weaken during negative SAM and El Niño events. Such interactions have far-reaching implications for the regional atmospheric and ocean circulations and sea ice (Turner et al., 2013; Raphael et al., 2016). Additionally, a negative (positive) IPO leads to cooler (warmer) SSTs in the Ross, Amundsen and Bellingshausen seas and has the potential to strengthen (in phase) or weaken (out of phase) the ENSO teleconnection (Henley et al., 2015). Furthermore, the phasing and strength of ENSO events and SAM have been shown to be time dependent (Fogt and Bromwich, 2006).
Our data suggest that changes in these dynamically linked climate patterns coincide with significant and abrupt changes in the past with implications for regional interpretations of trends, including temperature, mass balance and SIE. For over 2 kyr, from 660 BCE to the late 14th century, climate trends in the eastern Ross Sea (RICE and Siple Dome, trend to warmer isotope temperatures and higher precipitation) are anti-correlated with conditions in western West Antarctica (WDC, isotopic cooling with reduced precipitation), while coastal East Antarctica in the western Ross Sea appeared decoupled (there was no trend in isotope temperature or precipitation at TALDICE/Taylor Dome and Talos Dome, respectively). This regional pattern was reorganised during a period with strongly negative SAM conditions (SAMA) accompanied by exceptionally warm tropical SST (Niño 3.4 index). In modern times, such conditions cause a weakening of the ASL, which in turn can lead to a reduction in marine air mass intrusions into West Antarctica. Indeed, we observe that western West Antarctica (WDC borehole and isotope temperature) and the western Ross Sea (TALDICE) show cold temperatures during this time period that coincides with the Little Ice Age, while the eastern Ross Sea (RICE, Siple Dome) shows warmer or stable-isotope temperatures. In the late 17th century, the SAMA changes to above-average values, concurrent with a change to strong La Niña-like conditions, a framework conducive to a deepening of the ASL. Now, West Antarctica (WDC borehole temperature), the eastern Ross Sea (RICE, Siple Dome) and the western Ross Sea (TALDICE) all experience warmer isotope temperatures. At the same time, however, we observe reduced snow accumulation at RICE and WDC and an increase at Talos Dome. We interpret this pattern to reflect an increase in SIE in the eastern Ross Sea with perhaps the establishment of the modern Roosevelt Island polynya as a local moisture source for RICE. The continued improvements of array reconstructions (Stenni et al., 2017; Thomas et al., 2017) and the assessment of isotope-enabled climate models are an exciting development to further our knowledge of the drivers and effects of past change and their implications for future projections.
The following new RICE data are made available in this paper:
RICE water stable isotopes (δD) have been archived at the PANGAEA data base: https://doi.org/10.1594/PANGAEA.880396 (Bertler et al., 2017).
GPS and radar data have been archived at the U.S. Antarctic Program Data Center: https://gcmd.gsfc.nasa.gov/search/Metadata.do?entry=USAP-0944307&subset=GCMD (Kingslake et al., 2014; Matsuoka et al., 2015).
The following published RICE data used in this paper are accessible in the following way:
RICE17 age scale has been archived at the PANGAEA data base: https://doi.org/10.1594/PANGAEA.882202 (Winstrup and Vallelonga, 2017).
RICE snow accumulation data have been archived at the PANGAEA data base: https://doi.org/10.1594/PANGAEA.882202 (Winstrup and Vallelonga, 2017).
Sources of published ice core data used in this paper are as follows:
WDC water stable isotopes (δ18O) were accessed via https://www.nature.com/articles/nature12376#supplementary-information (WAIS Divide Project Members, 2013).
WDC snow accumulation data were accessed via http://www.usap-dc.org/view/dataset/601004 (Fudge et al., 2016).
WDC borehole temperature was accessed via https://nsidc.org/data/NSIDC-0638/versions/1 (Orsi et al., 2012).
Talos Dome snow accumulation data were accessed via https://www.ncdc.noaa.gov/paleo/study/22712 (Stenni et al., 2002).
TALDICE water stable-isotope data (δ18O) were accessed via https://www1.ncdc.noaa.gov/pub/data/paleo/pages2k/stenni2017antarctica/ (Stenni et al., 2017).
Siple Dome water stable isotopes (δ18O) were accessed via https://www.nature.com/articles/nature12376#supplementary-information (WAIS Divide Project Members, 2013).
Taylor Dome water stable isotopes (δ18O) were accessed via https://www1.ncdc.noaa.gov/pub/data/paleo/pages2k/pages2k-temperature-v2-2017/data-current-version/Ant-TaylorDome.Steig.2000.txt (Steig et al., 2000).
Sources of meteorological data and climate indices used in this paper are as follows:
SAMA developed by Abram et al. (2014) was accessed via ftp://ftp.ncdc.noaa.gov/pub/data/paleo/contributions_by_author/abram2014/abram2014sam.txt.
The Niño 3.4 Index developed by Emile-Geay et al. (2013) was accessed via ftp://ftp.ncdc.noaa.gov/pub/data/paleo/contributions_by_author/emile-geay2012/emile-geay2012.xls.
The Niño 3.4 Index (Rayner et al., 2003a) was accessed via http://www.esrl.noaa.gov/psd/gcos_wgsp/Timeseries/Nino34/.
The Niño 4 Index (Rayner et al., 2003a) was accessed via https://www.esrl.noaa.gov/psd/gcos_wgsp/Timeseries/Nino4/.
SOI (Allan et al., 1991) was accessed via http://www.cru.uea.ac.uk/cru/data/soi/.
The Ross–Amundsen Sea SIEJ developed by Jones et al. (2016) was accessed via http://www.nature.com/articles/nclimate3103#supplementary-information.
Byrd Station meteorological data (Bromwich et al., 2013) were accessed via the Byrd Polar Research Centre, Polar Meteorological Group, Ohio State University: http://www.polarmet.osu.edu/datasets/Byrd_recon/.
Meteorological data for Ferrell, Gill and Margaret AWS were accessed via the Antarctic Meteorological Research Center and Automatic Weather Station Project https://amrc.ssec.wisc.edu.
Data for McMurdo Station and Scott Base are accessed via the MET-READER: https://legacy.bas.ac.uk/met/READER/data.html (Turner et al., 2004).
The IPO Index (Henley et al., 2015) was accessed via http://www.esrl.noaa.gov/psd/data/timeseries/IPOTPI/.
NB2014 were accessed via http://polarmet.osu.edu/datasets/Antarctic_recon/ (Nicolas and Bromwich, 2014).
The supplement related to this article is available online at: https://doi.org/10.5194/cp-14-193-2018-supplement.
The authors declare that they have no conflict of interest.
Funding for this project was provided by the New Zealand Ministry of
Business, Innovation, and Employment Grants through Victoria University of
Wellington (RDF-VUW-1103, 15-VUW-131) and GNS Science (540GCT32, 540GCT12),
and Antarctica New Zealand (K049), the US National Science Foundation (US
NSF ANT-0944021, ANT-0944307, ANT-1443472), British Antarctic Survey Funding
(BAS PSPE), the Center of Ice and Climate at the Niels Bohr Institute
through the Carlsberg Foundation's “North-South Climate Connection”
project grant, and the Major State Basic Research Development Program of
China (Grant No. 2013CBA01804). The authors appreciate the support of the University
of Wisconsin-Madison Automatic Weather Station Program for the data set,
data display and information (NSF grant number ANT-1543305). We are indebted to Hedley Berge, Jeff
Rawson, Margie Grant, Lou Albershardt, and Antarctica New Zealand staff at
Scott Base and in Christchurch for their support of the RICE field seasons.
We are grateful for the support by US 109th New York Air National Guard
(NYANG) LC-130 Hercules and Canadian Kenn Borek aircraft crews for their
excellent support into and out of Roosevelt Island. Furthermore, we would
like to thank Stephen Mawdesley, Grant Kellett, Ryan Davidson, Ed
Hutchinson, Bruce Crothers and John Futter of the Mechanical and Electronic
Workshops of GNS Science for technical support for the international RICE
core progressing campaigns. We would like to thank Beaudette Ross for
conducting gas isotope measurements at the Scripps Institution of
Oceanography, University of California, San Diego. We are grateful to Diane
Bradshaw and Bevan Hunter for their assistance in naming the New Zealand ice
core drill. We would like to thank Barbara Stenni for advice and discussions
on the Talos Dome and TALDICE records. We thank two anonymous reviewers to
help us make important improvements to this paper. This work is a
contribution to the Roosevelt Island Climate Evolution (RICE) Program,
funded by national contributions from New Zealand, Australia, Denmark,
Germany, Italy, the People's Republic of China, Sweden, the UK and the USA.
Logistics support was provided by Antarctica New Zealand (K049) and the US
Edited by: Hugues Goosse
Reviewed by: two anonymous referees
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