Introduction
East Antarctica is characterized by a long winter (>10 months) with extremely low temperatures and strong winds. Due to temperature inversion near the surface and the sloping topography of the ice sheet, intense and directionally constant katabatic winds develop, which are accelerated in regions with confluent topography (Reference Parish and BromwichParish and Bromwich, 1987). Due to its extreme climate, with probably the strongest near-surface winds on Earth, Terre Adélie (Fig. 1) and its surroundings is an interesting topic for scientific studies. Conversely, these extreme conditions make it hard to perform in situ measurements. Reference Wendler, Stearns, Weidner and DargaudWendler and others (1997) described 4 months of wind speed measurements (until the instruments broke during a storm) in coastal Terre Adélie (Cape Denison). These data confirm that the highest annual mean wind speed (19.1 ms-1), measured by Reference MawsonMawson (1915) and corrected by Reference LoeweLoewe (1972), occurs here. Reference Wendler, Stearns, Weidner and DargaudWendler and others (1997) also found that the spatial variability is large on scales of tens of kilometers, owing to rough topography with alternating valleys and ridges: for instance, the annual mean wind speed at the French station Dumont d'Urville (situated 120 km west of Cape Denison on a small island 2 km offshore) is only 9.5 m s-1.
Fig. 1. Overview of model domain. Model topography is shown in colors, with scale ranging from 0 to 4000ma.s.l. The position of the model domain on the Antarctic ice sheet is indicated in the inset. The locations and names of the AWSs used for wind speed evaluation (Nos. 1 to 11, Fig. 3) are also given, together with the location of Talos Dome (Fig. 5).
Topography in Antarctica strongly controls not only the wind climate, but also the spatial variability of snow accumulation, sublimation and erosion, which are all components of the surface mass balance (SMB). Most importantly, SMB strongly decreases from the coast to the Antarctic plateau, but it also varies on much smaller scales (Reference Van de Berg, Van den Broeke, Reijmer and Van MeijgaardVan de Berg and others, 2006; Reference AgostaAgosta and others, 2012; Reference Lenaerts and Van den BroekeLenaerts and others, 2012a). The SMB at a specific location (units mm w.e. a-1 or kg m-2 a-1) is defined as
where P is precipitation (snow and rain), SUs is surface sublimation, RU is runoff from rainfall, snow and ice melt, and ERds and SUds represent drifting snow erosion and sublimation, respectively. Due to low temperatures, significant rainfall and runoff do not occur in East Antarctica and SUs is small. Snowfall is generally low; as a result, most of the East Antarctic plateau has an annual SMB <50 mm w.e. a-1 (Reference Lenaerts and Van den BroekeLenaerts and others, 2012a), increasing to typically 200-500 mm w.e. a-1 in the coastal regions. Because of the dry climate, drifting snow sublimation, SUds, and erosion, ERds, may remove a significant part of the accumulated snow (Reference FrezzottiFrezzotti and others, 2004), and may even lead to ablation (SMB < 0) in the driest and windiest regions (Reference BintanjaBintanja, 1999; Reference Van de Berg, Van den Broeke, Reijmer and Van MeijgaardVan den Broeke and others, 2006; Reference Genthon, Lardeux and KrinnerGenthon and others, 2007; Reference Lenaerts and Van den BroekeLenaerts and Van den Broeke, 2012). Remotely sensed observations show that drifting snow events occur frequently in East Antarctica (Reference Mahesh, Eager, Campbell and SpinhirneMahesh and others, 2003), evidenced by the presence of large-scale snow 'billows' and dunes after these events (Reference Scarchilli, Frezzotti, Grigioni, De Silvestri, Agnoletto and DolciScarchilli and others, 2010). Moreover, during strong events, drifting snow layers may become as deep as, or deeper than, 200 m (Reference Palm, Yang, Spinhirne and MarshakPalm and others, 2011). Therefore, it is essential to include drifting snow physics when we simulate the East Antarctic climate and SMB (Reference Frezzotti, Gandolfi and UrbiniFrezzotti and others, 2002, Reference Frezzotti2007; Reference Gallée, Peyaud and GoodwinGallée and others, 2005; Reference Scarchilli, Frezzotti, Grigioni, De Silvestri, Agnoletto and DolciScarchilli and others, 2010; Reference AgostaAgosta and others, 2012).
Because of the impact of topography, many atmospheric processes occur on scales smallerthan the typical horizontal resolution of atmospheric or climate models. In Antarctica, the spatial variability of precipitation is largely determined by topography (Reference BromwichBromwich, 1988), because of the dominant contribution of orographic precipitation. This enhances precipitation on the windward side of topographic features. Topography is smoothed as grid size increases, and as a result, SMB becomes a function of a model's horizontal resolution (Reference Genthon, Krinner and CastebrunetGenthon and others, 2009). The slope in topography also determines the strength of the katabatic wind and resulting drifting snow. Snowdrift erosion, ERds, represents the horizontal divergence of the wind transport of snow (Reference Lenaerts and Van den BroekeLenaerts and others, 2012b) and strongly depends on spatial variations in wind speed. Reference Lenaerts and Van den BroekeLenaerts and Van den Broeke (2012) demonstrated that, at a horizontal resolution of 27 km, ERds is only significant (>10 mm w.e. a-1) on a regional scale, but we expect its importance to become more pronounced at higher resolution. An example is the presence of so-called megadunes, typical of interior East Antarctica. Megadunes have a typical wavelength of 510 km and their development is presumably related to small-scale variations in wind speed (Reference Fahnestock, Scambos, Shuman, Arthern, Wine-brenner and KwokFahnestock and others, 2000; Reference Frezzotti, Gandolfi and UrbiniFrezzotti and others, 2002). In this paper, we discuss the impact of horizontal resolution on the representation of the wind climate and SMB of eastern East Antarctica (135-180° E), including Terre Adélie, Victoria Land and most of Wilkes Land. We run the regional atmospheric climate model RACMO2.1/ANT for 1 year (2009) at high horizontal resolution (5.5 km). We compare the wind climate, drifting snow climate and SMB with the output of the previous run with the same model version at 27 km (Reference Lenaerts and Van den BroekeLenaerts and others, 2012b), and evaluate the differences using available observations.
Methods
Numerical set-up
For the purpose of this study we use the Regional Atmospheric Climate MOdel version 2.1 (RACMO2.1/ANT). RACMO2.1/ANT combines the dynamical processes of the High Resolution Limited Area Model (HIRLAM; Reference UndénUndén and others, 2002) with the physical parameterizations from the European Centre for Medium-Range Weather Forecasts (ECMWF) model Cycle 23r1 (Reference WhiteWhite, 2001). The latest version contains a multilayer snow model (Reference EttemaEttema and others, 2009) and a snow albedo scheme based on snow grain size (Reference Kuipers Munneke, Van den Broeke, Lenaerts, Flanner, Gardner and Van de BergKuipers Munneke and others, 2011). Additionally, a drifting snow routine is included in RACMO2.1/ANT, which is based on the bulk drifting snow routine of Dery and Yau (1999). The routine uses wind speed, temperature and specific humidity at the lowest model level (˜7m) to calculate drifting snow sublimation, SUds, and transport, TRds. Assuming it is the only source of latent heat during drifting snow, the effect of SUds on the near-surface atmosphere is explicitly included in RACMO2.1/ANT. Moreover, both SUds and ERds are included as explicit terms in the SMB scheme of RACMO2.1/ANT (Eqn (1)). By removing or depositing mass from the top snow layer, both processes can impact its density, which, in turn, limits the potential for drifting snow (Reference Lenaerts and Van den BroekeLenaerts and others, 2012b).Reference Lenaerts and Van den BroekeLenaerts and others (2012b) provide additional details of the numerical set-up and a detailed evaluation of the near-surface climate and drifting snow characteristics. Among other things, they show that the model, with a horizontal resolution of 27 km, is able to realistically simulate the near-surface climate (Reference Lenaerts and Van den BroekeLenaerts and Van den Broeke, 2012) and SMB (Reference Lenaerts and Van den BroekeLenaerts and others, 2012a) of the Antarctic ice sheet, without the need for post-calibration.
Here we further increase the horizontal resolution of RACMO2.1/ANT, from 27km (RACMO/27 hereafter) to 55 km (RACMO/5.5 hereafter), to better resolve the complex topography of East Antarctica and related interactions with the atmosphere. The model domain encompasses the eastern part of East Antarctica (Fig. 1). The lateral boundaries are chosen to minimize crossing distinct topography. The atmospheric fields at these boundaries are provided by RACMO2.1/ANT at 27 km resolution, such that the effect of downscaling the atmospheric fields at the lateral boundaries remains small. Sea-ice extent and sea surface temperature are prescribed from ERA Interim reanalysis data (Reference DeeDee and others, 2011). Because of the exploratory nature of this work and the high computational cost, we ran the model for a single year (2009). The snowpack is initialized with data from 1 January 2009 from RACMO/27. Model elevation in RACMO2.1/ANT is constant, which is a reasonable assumption considering the temporal scale (1 year) of this study.
Observational data
The near-surface climate of East Antarctica is monitored by different automatic weather stations (AWSs), which sample wind speed and direction at 3 or 10 m above the surface at hourly or sub-hourly resolution. Here we evaluate the model results for the AWSs located in rough topography and with high wind speeds (>9ms-1). Figure 1 shows the locations and names of these stations. All wind-speed data are converted to a standard height of 10m (Reference Sanz RodrigoSanz Rodrigo, 2011).
At daily resolution, the modeled wind speed is compared with observational data (see Fig. 2 for locations) from AWSs at Larsen Glacier (a; 75° S, 161° E, 1350 m a.s.l.), Sitry (b; 72° S, 149° E, 2094 m a.s.l.), Priestley Glacier (c; 74° S, 162° E, 1923 m a.s.l.) and David Glacier (d; 76° S, 159° E, 1552 m a.s.l.), obtained from the Meteo Climatological Observatory of PNRA (Programma Nazionale di Ricerche in Antartide; http://www.climantartide.it). The first two stations are situated in the convergence slope/coastal areas of northern Victoria Land, whereas the latter two are located on the East Antarctic plateau (Fig. 1).
Fig. 2. Modeled annual mean (2009) 10m wind speed (contours) and direction (arrows) in RACMO/5.5 (left) and RACMO/27 (right). The locations of the four AWSs in Figure 4a–d are indicated by their respective letters.
Drifting snow measurements are sampled at the Talos Dome TALDICE drilling site (72° S, 159° E, 2315m a.s.l.; http://www.taldice.org; see Fig. 1 for location). Measurements are obtained with FlowCapt™ driftometer sensors produced by ISAW Outdoor Environmental Monitoring (Reference Chritin, Bolognesi and GublerChritin and others, 1999). The instrument is composed of four sensors: two of these are placed 0.2 m above the snow surface, and the other two 1 m above the surface. These instruments provide inaccurate estimates of the snow transport fluxes (Reference Cierco, Naaim-Bouvet and BellotCierco and others, 2007), but do provide a realistic estimate of the occurrence of drifting snow.
Modeled SMB is compared with observations described by Reference AgostaAgosta and others (2012). The observations originate from a ˜150km long stake line that runs from the coast of Terre Adélie to the southwest (0-1800 m a.s.l.). Comparing RACMO to these observations can be regarded as a stringent test for model performance, because the stake line covers the strong SMB gradient between the relatively mild and windy coastal climate and drier and calmer conditions inland at high spatial resolution (100 data points).
Results
Wind climate
Figure 2 compares annual mean 10 m wind speed of RACMO/27 with RACMO/5.5. Although RACMO/5.5 obviously shows much more detail, the regional patterns are similar. We find four areas of strong (>14 ms-1) winds: three over outlet glaciers (Byrd, Mulock and Reeves/David Glaciers) in the Transantarctic Mountains, with several jets above 10 ms-1, and one in coastal Terre Adélie, with a maximum wind speed of 16ms-1 at ˜69° S, 143° E, 1100m a.s.l. On the smaller scale, the RACMO/5.5 wind field shows distinct features. Maximum wind speeds are higher and occur closer to the grounding line. Relatively narrow (<20 km) glacial valleys, in which the katabatic wind speeds converge and accelerate, are much better resolved at 5.5 km. In our simulation the strongest winds are found in the glacial valley of Reeves Glacier, with a maximum wind speed of 20.5 ms-1, and, to a lesser extent, David Glacier near the Italian base (Mario Zuchelli) in Terra Nova Bay (˜75° S, 163° E), and Byrd Glacier (81° S, 158° E). The occurrence of these maxima is supported by results of Reference Bromwich, Parish and ZormanBromwich and others (1990), who showed that Reeves Glacier is the primary route for katabatic winds, and David Glacier is an important secondary outflow valley.
Reference Lenaerts and Van den BroekeLenaerts and others (2012b) showed that RACMO/27 underestimates high wind speeds in regions with complex topography. Figure 3 illustrates that in these regions, wind speeds in RACMO/5.5 agree better with observations. The root-mean-square error (rmse) decreases from 5.7 ms-1 to 3.6 ms-1, and the mean bias between model and observations drops from −4.3 ms-1 to −1.4 ms-1. Nonetheless, the extreme wind speeds (>15 m s-1) in Terre Adélie remain underestimated.
Fig. 3. Modeled mean (2009) vs observed (mean of instrumental record; Reference Sanz RodrigoSanz Rodrigo, 2011) 10mwind speed for RACMO/5.5 (dots) and RACMO/27 (triangles), located in Victoria Land (red) and Terre Adélie (blue). The RACMO wind speeds are weighted averages of the four gridpoints surrounding the location of the AWS. Only AWSs with mean observed 10m wind speed >9ms-1 are shown. Their locations and names are given in Figure 1.
Figure 3 only shows long-term mean near-surface wind speeds. Drifting snow processes, however, are usually connected to short-lived wind speed maxima. To evaluate the model results at higher temporal resolution, Figure 4 shows the daily mean 10m wind speed from RACMO/5.5, RACMO/27 and from available AWS observations. Due to limited temporal coverage and large gaps in the data, these AWSs are not included in Figure 3. At daily resolution, RACMO/5.5 shows clearly higher maximal wind speeds than RACMO/27 at all stations, except for Sitry (Fig. 3b), where topography is smooth and the model agrees very well with the observations, even at 27 km resolution. The other three stations are known to be major confluence areas, where the katabatic wind accelerates due to the convex shape of the glacier valley (Reference Bromwich, Rogers, Kållberg, Cullather, White and KreutzBromwich and others, 2000). At Larsen Glacier, the modeled timing and frequency of wind speed maxima agree very well with the observations, whereas at Priestley and David Glaciers, observed wind speed maxima remain largely underestimated, also by RACMO/5.5. The intense local katabatic flow at these locations is likely driven by topographic features at scales smaller than the model resolution of 5.5 km, as also reported by Reference Scarchilli, Frezzotti, Grigioni, De Silvestri, Agnoletto and DolciScarchilli and others (2010).
Fig. 4. Modeled daily mean (2009) vs observed (black dots) 10m wind speed for RACMO/5.5 (red) and RACMO/27 (blue). The RACMO wind speeds are weighted averages of the four gridpoints surrounding the location of the AWS. The AWS locations are shown in Figure 2. Note that there are significant gaps in the observational data for all stations.
Drifting snow
Figure 5 presents a comparison of observed and modeled occurrence of drifting snow at Talos Dome during winter 2009. This site is characterized by a cold, windy climate: the modeledmean air temperature is 229 K and the average near-surface wind speed is 8.5ms-1 during the period shown in Figure 5 (May–August 2009). Figure 5 shows that drifting snow occurs frequently at Talos Dome. The model simulates a drifting snow frequency of 58%, whereas the observations indicate that on 67% of the days drifting snow occurs. The model agrees with the observations on the timing and duration of especially the strongest drifting snow events, whereas some weaker events are not picked up, or their duration is underestimated (e.g. the long event at the end of May is not modeled). In total, 59% of the observed events are also modeled, whereas 30% of the modeled events are false detections. Unfortunately, no reliable drifting snow transport observations are available for comparison. This illustrates the need for more detailed in situ observations of drifting snow.
Fig. 5. Modeled and observed drifting snow occurrence (markers) at Talos Dome during the period May–August 2009, and modeled horizontal snow transport, TRds, during that period (red bars). The location of Talos Dome is shown in Figure 1.
Reference Lenaerts and Van den BroekeLenaerts and Van den Broeke (2012) discussed the drifting snow climate of Antarctica as simulated in RACMO/27. They found SUds values up to 150 mm w.e. a-1 in coastal areas of East Antarctica. Because of the underestimation of the highest wind speeds in RACMO/27 (Fig. 3), a problem that is greatly reduced at higher horizontal resolution (Fig. 3), higher SUds (Fig. 6a) and transport (not shown) are simulated in RACMO/5.5. SUds exceeds 70 mm w.e. a-1 in large parts of coastal Terre Adélie, with peak values >300 mm w.e. a-1. Similar values are found in the glacial valleys in Victoria Land where katabatic outflow is strongest (Fig. 2).
Fig. 6. Total (a) SUds and (b) ERds in 2009 as modeled byRACMO/5.5. The location transect shown in Figure 7 is shown by the thick black line.
Drifting snow erosion, ERds, represents the divergence of horizontal snow transport, TRds. From a modeling perspective, this implies that ERds is largely determined by how well the topography is resolved, i.e. by the horizontal grid size. Figure 6b presents ERds for 2009. On the model grid, ERds shows large variability, ranging from —100 to + 100 mm w.e. in 2009. In RACMO/27 we find only small values of ERds (not shown; Reference Lenaerts and Van den BroekeLenaerts and Van den Broeke, 2012). In order to analyze these differences in more detail, we focus on a horizontal cross section through an area with strong variability in drifting snow erosion (70-72° S, 148.5° E; Fig. 6b). Along the transect, the elevation decreases from 2120 to 1550 m a.s.l. (Fig. 7a). The elevation in RACMO is derived from the 5 km resolution RADARSAT-1 Antarctic Mapping Project (RAMP) digital elevation model (DEM) (Reference Liu, Jezek, Li and ZhaoLiu and others, 2001), whereas Figure 7a shows the most recent Antarctic DEM (Reference Bamber, Gomez-Dans and GriggsBamber and others, 2009) at 1 km resolution. For unknown reasons, the elevation in the RAMP DEM in this region is significantly offset, by ˜60 m, in comparison with the DEM of Reference Bamber, Gomez-Dans and GriggsBamber and others (2009). From the various elevation datasets, we derived the slope as represented in RACMO/27, RACMO5.5 and the 1 km DEM (Fig. 7b). In all cases, the slope magnitude increases along the transect. The slope in RACMO/5.5 shows larger variability than in RACMO/27, but has smaller variability than the 1 km DEM. This implies that important subgrid topographical variability exists that is not resolved by either regional climate model. Although smoothed, RACMO/5.5 captures the spatial variability in slope relatively well.
Fig. 7. Horizontal cross section through Terre Adélie (see Fig. 6 for location) of (a) surface elevation, (b) total surface slope in the 1 km DEM (Reference Bamber, Gomez-Dans and GriggsBamber and others, 2009), RACMO/5.5 and RACMO/27, (c) 10m wind speed and (d) ERds in 2009 from RACMO/5.5 and RACMO/27.
Along the transect, 10 m wind speed variations (Fig. 7c) are strongly correlated with the slope, a feature not resolved at 27km resolution. This has a profound impact on the spatial variations in drifting snow erosion (Fig. 7d). Whereas ERds is not significant in RACMO/27, ERds values of —60 to +90mmw.e. a-1 are found in RACMO/5.5. Generally, ERds is most negative (positive) just before the strongest wind speed acceleration (deceleration). This illustrates the tight coupling between surface slope, wind speed and drifting snow processes (and their impact on SMB) in katabatic wind regions.
Surface mass balance
Figure 8 compares the observed and modeled SMB along the stake line, whose location is shown by 'S' in Figure 9. RACMO/5.5 performs better than RACMO/27, although SMB remains overestimated near the coast. The strong SMB decrease between 30 and 90km from the coast is better represented at 5.5 km resolution. The mean SMB bias is greatly reduced from +222 (63%) to —12 mm w.e. a-1 (3%), for two reasons: firstly, SUds increases by ˜100mmw.e., a direct result of higher, more realistic near-surface wind speeds in RACMO/5.5; secondly, snowfall is clearly reduced at 5.5 km resolution (Fig. 8b), because topography is better represented, inducing more snowfall on the upwind side of the ridges (around 145° E; Fig. 9) and less snowfall behind these features. It is likely that drifting snow processes are even more important in the coastal regions than modeled by RACMO/5.5. Reference Genthon, Lardeux and KrinnerGenthon and others (2007) described the characteristics of the blue-ice area located just off the coast, and concluded that, in ablation years such as 2009, SUds and ERds remove all accumulated snow, due to the local shape and/or steeper slope of the blue-ice area. This would suggest that ERds due to model resolution is still poorly represented by RACMO/5.5 in this region, since it produces a net convergence of snow in response to weaker winds just before the ice-sheet/ocean interface (Fig. 8).
Fig. 8. (a) SMB in 2009 measured by stakes (Reference AgostaAgosta and others, 2012) and modeled by RACMO/5.5 (dashed curve) and RACMO/27 (dotted curve). The spatial resolution is 5.5 km, and the modeled data are weighted averages of the four surrounding gridpoints. The vertical dashed bars represent one spatial standard deviation of the observations in both directions. (b) Snowfall, (c) ERdsand (d) SUdsin 2009, modeled by RACMO/5.5 (dashed curve) and RACMO/27 (dotted curve).
Fig. 9. SMB in 2009 as modeled by RACMO/5.5 (left) and RACMO/27 (right). Note that the 5.5 km resolution coastline and topography is shown in both plots. The location of the stake line ('S') is also shown in both plots.
Reference Fahnestock, Scambos, Shuman, Arthern, Wine-brenner and KwokLenaerts and others (2012a) present the modeled SMB from RACMO/27, and found excellent agreement between modeled and observed SMB. However, they found a negative bias in RACMO/27 in northern Victoria Land, which may be attributed to clear-sky precipitation that is not simulated. A similar SMB underestimation is found in RACMO/5.5; compared with the ground-penetrating radar observations of Reference Frezzotti, Urbini, Proposito, Scarchilli and GandolfiFrezzotti and others (2007) near Talos Dome, the modeled SMB is ˜30mmw.e. a-1, whereas the stakes suggest an annual SMB of ˜90 mm w.e. In the near future, an improved precipitation scheme will be included in RACMO that will likely decrease this bias.
Figure 9 compares the 2009 SMB in RACMO/5.5 and RACMO/27. The large-scale patterns are again similar. Clearly, the spatial variability is larger in RACMO/5.5. Along the Terre Adélie coast we find high SMB values (>1000 mm w.e. a-1 in RACMO/5.5) on the east-facing (upwind) topographic ridges, whereas SMB is much lower on the lee sides (<500 mm w.e. a-1 in RACMO/5.5). Even larger gradients (>1500 mm w.e.) are modeled along the northern coast of Victoria Land (around 72° S, 170° E). This large-scale variability is explained by the strong control of topography on precipitation.
Negative SMB (ablation) is found in large parts of Victoria Land in both simulations. This ablation area is more widespread and patchy in RACMO/5.5, because of the large spatial variations in drifting snow erosion. Regions with similarly alternating patterns of accumulation (SMB > 0) and ablation (SMB < 0) occur where ERds strongly varies (Fig. 6b). These patterns have a typical wavelength of ˜10-20km, and are aligned perpendicular to the prevailing wind direction. They represent the steady-state interaction of topography with the atmosphere, as snow converges in front of a dune and is eroded and sublimated away behind it.
Table 1 presents the spatially integrated SMB and its components. Although the SMB difference between RACMO/5.5 and RACMO/27 is locally large, we find no significant change in domain-integrated SMB; it decreases from 90Gt to 86 Gt in 2009. SUdsis the only SMB component that significantly increases with increasing horizontal resolution. In RACMO/27 it is 14% of the snowfall, and this increases to 21% of the snowfall at 5.5 km resolution. In contrast, SUsdecreases by 50% in RACMO/5.5. The integrated ERds remains negligible (<1 Gt) at higher horizontal resolution.
Table 1. Domain-integrated values for the year 2009 of snowfall, rainfall, melt, runoff, refreezing, drifting snow sublimation (SUds), surface sublimation (SUs), total sublimation (SUtot = SUds + SUs) and SMB (SMB) for the RACMO/5.5 and RACMO/27 simulations
Ablation also occurs in large glacial valleys (Fig. 9), where modeled near-surface wind speeds are high (Fig. 2). In these valleys, drifting snow processes are key components of the SMB. Figure 10 shows the SMB and its components along a transect that approximately follows the center line of Byrd Glacier, whose surface largely consists of blue ice. Figure 10b reveals that along the narrow part of the glacial valley, which is ˜20 km wide and ˜75 km long (Reference Stearns, Smith and HamiltonStearns and others, 2008; Fig. 10a), drifting snow erosion, ERds, quickly increases from —300 to +200 mm w.e., as a result of acceleration of the near-surface flow. In the same area, SUds increases to peak values >300 mm w.e. This results in a clearly negative SMB (<—100 mm w.e.) along the whole narrow part of the glacial valley. At ˜162° E, where Byrd Glacier terminates into the Ross Ice Shelf, near-surface wind speed decreases and SMB becomes positive again. At 27 km resolution, these small-scale features are not represented. Reference StearnsStearns (2011) pointed out that earlier estimates (e.g. Reference Van de Berg, Van den Broeke, Reijmer and Van MeijgaardVan de Berg and others, 2006) overestimate SMB in the Byrd Glacier catchment. Our results suggest that the inclusion of ERds and SUds, along with the higher resolution in RACMO/5.5, leads to a lower, more realistic SMB for this region.
Fig. 10. SMB from RACMO/5.5 along Byrd Glacier. (a) Colors: SMB and location of the transect; black lines: height contours at 500m resolution. (b) SMB and its components along the transect.
Conclusions
We have described the impact of model resolution on the simulated wind climate, drifting snow and SMB of Terre Adélie and its surroundings. For this purpose, we used the single-year (2009) output of a regional atmospheric climate model at high horizontal resolution (5.5 km) and compared this with earlier results at 27km resolution. Because the topography is much better resolved at 5.5 km, the impact on the simulated climate is significant. Firstly, the near-surface wind speeds are in better agreement with observations in areas with rough topography. We find the strongest annual mean near-surface winds in coastal Terre Adélie (16 ms-1) and especially in the narrow glacial valleys in Victoria Land (Byrd, Mulock and David Glaciers; up to 20.5 ms-1). Horizontal variations in slope magnitude, which are partly resolved at 5.5 km but not at 27km, result in horizontal wind speed gradients, which in turn lead to strong variability (—100 to +100 mm w.e.) of modeled drifting snow erosion, ERds. SUds is mainly dependent on wind speed, and is therefore significant in large parts of coastal Terre Adélie (>100 mm w.e.) and along the fast-flowing part of the large East Antarctic glaciers that terminate in the Ross Ice Shelf or Ross Sea.
SMB variability is largely determined by topography, on the large scale (where orographic precipitation is the dominant mechanism), as well as on model gridscale, where we find alternating patterns of ablation (SMB < 0) and accumulation (SMB > 0) that are controlled by ERds. Due to the high wind speeds, drifting snow (ERds and SUds) also leads to ablation in narrow glacier valleys that connect the East Antarctic ice sheet with the Ross Ice Shelf/Sea. We compared modeled SMB with observations along a stake line in Terre Adélie. Although SMB is overestimated at the coast and underestimated further inland, the spatial variability is well represented, and mean SMB bias along the stake line is largely reduced at 5.5 km (3%) compared with 27 km (63%). The spatially integrated SMB is estimated at 86 Gt for 2009, and is not significantly affected by the horizontal resolution.
Acknowledgements
We thank Thomas Mölg and two anonymous reviewers for valuable comments that considerably improved the paper. This work was supported by funding from the ice2sea programme through the European Union 7th Framework Programme, grant No. 226375. This is Ice2sea contribution No. 091.
