An indicator of sea ice variability for the Antarctic marginal ice zone
- 1Department of Oceanography, University of Cape Town, 7701, Rondebosch, South Africa
- 2Marine and Antarctic Research centre for Innovation and Sustainability (MARIS), University of Cape Town, 7701, Rondebosch, South Africa
Correspondence: Marcello Vichi (firstname.lastname@example.org)
Remote-sensing records over the last 40 years have revealed large year-to-year global and regional variability in Antarctic sea ice extent. Sea ice area and extent are useful climatic indicators of large-scale variability, but they do not allow the quantification of regions of distinct variability in sea ice concentration (SIC). This is particularly relevant in the marginal ice zone (MIZ), which is a transitional region between the open ocean and pack ice, where the exchanges between ocean, sea ice and atmosphere are more intense. The MIZ is circumpolar and broader in the Antarctic than in the Arctic. Its extent is inferred from satellite-derived SIC using the 15 %–80 % range, assumed to be indicative of open drift or partly closed sea ice conditions typical of the ice edge. This proxy has been proven effective in the Arctic, but it is deemed less reliable in the Southern Ocean, where sea ice type is unrelated to the concentration value, since wave penetration and free-drift conditions have been reported with 100 % cover. The aim of this paper is to propose an alternative indicator for detecting MIZ conditions in Antarctic sea ice, which can be used to quantify variability at the climatological scale on the ice-covered Southern Ocean over the seasons, as well as to derive maps of probability of encountering a certain degree of variability in the expected monthly SIC value. The proposed indicator is based on statistical properties of the SIC; it has been tested on the available climate data records to derive maps of the MIZ distribution over the year and compared with the threshold-based MIZ definition. The results present a revised view of the circumpolar MIZ variability and seasonal cycle, with a rapid increase in the extent and saturation in winter, as opposed to the steady increase from summer to spring reported in the literature. It also reconciles the discordant MIZ extent estimates using the SIC threshold from different algorithms. This indicator complements the use of the MIZ extent and fraction, allowing the derivation of the climatological probability of exceeding a certain threshold of SIC variability, which can be used for planning observational networks and navigation routes, as well as for detecting changes in the variability when using climatological baselines for different periods.
The Southern Ocean holds the largest circumpolar marginal ice zone (MIZ) in the global ocean (Weeks, 2010, p. 408), while the Arctic MIZ regions are mostly confined to the Bering Sea and the Greenland and Norwegian seas (Wadhams, 2000). In most general terms and independently of the hemisphere, the MIZ can be depicted as a band of young or fractured ice with floes smaller than a few hundred metres, which is continuously affected by air–sea interactions in the form of heat exchanges, wind and current drag, and wave action (Häkkinen, 1986; Dumont et al., 2011; Williams et al., 2013; Zippel and Thomson, 2016; Sutherland and Dumont, 2018; Squire, 2020).
1.1 Definitions of the MIZ: sea ice concentration, wave penetration and ice type
The MIZ is a transitional region, and as such, it is often defined by contrasting consolidated pack ice against open-ocean conditions. This implies the identification of two boundaries, one at the ice–ocean margin and one within the pack ice. The ocean edge and the MIZ extent are inextricably linked, since it is difficult to find sharp separations between these two components. Hence, the definition of the MIZ in the literature depends on the properties that are of interest in each study and often on the polar hemisphere considered. Following on from Arctic studies, the boundaries are derived from contour lines of sea ice concentration (SIC), the fraction of ice-covered water obtained through passive microwave sensors on board satellites (Comiso and Zwally, 1984; Meier and Stroeve, 2008/e; Strong and Rigor, 2013; Stroeve et al., 2016). Operationally, the MIZ is defined as that region of the sea ice where SIC comprises between 15 % and 80 %, and the MIZ extent depends on how the distance between these contours are computed (Strong et al., 2017). This definition is tightly linked to the SIC retrieval from satellites, since the limit of 15 % is considered to be a viable rule of thumb to overcome the uncertainties in the methodology (Comiso and Zwally, 1984). Within this range, sea ice is assumed to be in open-pack conditions, with higher chances of drifting ice and the penetration of gravity waves due to the floes being smaller than the wavelength (Squire, 2020). The threshold-based MIZ definition has been directly applied to Antarctic sea ice despite the remarkable differences in sea ice formation processes (e.g. Weeks and Ackley, 1986; Petrich and Eicken, 2017; Maksym, 2019). As an alternative definition, it has been proposed to estimate the MIZ extent based on the region where the wave field is responsible for setting the sea ice thickness (Williams et al., 2013; Sutherland and Dumont, 2018). Rolph et al. (2020) argue that, even if the use of more physical concepts such as the penetration of waves is a valid definition for studies of the MIZ, comparisons of MIZ extent between model and observational products should be based on SIC thresholds. The analysis of the MIZ fraction of the total cover based on SIC thresholds has shown promising results to benchmark the skill of climate models and their response to atmospheric warming (Horvat, 2021). Sea ice in the MIZ is therefore of a special kind, which responds differently than pack ice to the environmental drivers and may have relevant climatic implications, at least in the Arctic.
However, the relationship between SIC, ice type and ice properties is not yet constrained in the Southern Hemisphere. Ice type is still an ambiguous term in the literature because it is used differently in different contexts. In predominantly seasonal sea ice as found in the Antarctic, with continuous transition between new and young ice and the dominance of frazil ice (Matsumura and Ohshima, 2015; Haumann et al., 2020; Paul et al., 2021), the exchanges of energy across the interface may be less dependent on the degree of coverage and rather be more affected by the composite of the sea ice texture. Ice type is derived from direct observations, using categories like the WMO nomenclature and codes (WMO, 2014, 2021) and the SCAR Expert Group on Antarctic Sea-ice Processes and Climate, ASPeCt (https://www.scar.org/science/aspect/home/, last access: 1 September 2022). These classified features of sea ice heterogeneity do not necessarily covary with SIC or thickness, which means that young ice less than 30 cm thick with a combination of pancake and frazil ice can still have 100 % cover (Fig. 1c), which is susceptible to wave penetration. Wave attenuation is considered to be a function of ice type (ice properties), which is ultimately approximated to sea ice concentration (Mosig et al., 2015; Squire, 2020) for lack of better assumptions. This creates circular reasoning, since we are looking to define the MIZ extent based on waves that depend on ice properties that we cannot measure, and hence we resort to the observable variables: SIC, mean wave period and wind direction. Based on recent observations in the Ross Sea in autumn, Montiel et al. (2022) have found that simple parameterisations of attenuation are unlikely to capture the wide range of sea ice conditions found in the Southern Ocean.
It is no surprise that the SIC-based definition of the MIZ is thus the one most often used to estimate temporal trends in the MIZ extent at both poles (Strong and Rigor, 2013; Strong, 2012; Stroeve et al., 2016; Rolph et al., 2020; Horvat, 2021), with contrasting results that may be partly attributed to methodological issues (Strong et al., 2017). Stroeve et al. (2016) found large differences in estimating the seasonal cycle of the Antarctic MIZ extent using different algorithms. Over a climatological seasonal cycle, the bootstrap method returned a higher percentage of consolidated pack ice than the NASA Team algorithm, and this led to differences in the trend analyses.
1.2 Characterising variability in Antarctic sea ice
A most pressing question is not whether the MIZ has been increasing or decreasing in the Antarctic and how different it is from the Arctic but rather if the Antarctic MIZ features and variability can be properly captured using the threshold-based concentration criteria. With variability I refer to the daily change in SIC over a monthly scale in a climatological sense, and I will expand later on the roles of spatial and temporal variability. In the Antarctic, the MIZ is a characteristic of the advancing edge, since during this phase, sea ice progresses northwards and expands zonally due to the increase in ocean surface towards the Equator. This leads to divergence and lowers the chances of rafting and ridging, which are still considered the main thickening mechanisms in the Southern Ocean (Worby et al., 1996). An analysis of one ice-tethered buoy deployed in the East Antarctic sector revealed a large MIZ band of almost 300 km that persisted throughout the winter expansion until early December (Womack et al., 2022), with satellite-retrieved ice cover permanently above 100 %. In this region there would be no exchange through the ice between the ocean and the atmosphere, largely underestimating the possible fluxes. Almost all the proposed parameterisations of energy, momentum and gas exchange through sea ice are linearly dependent on the area cover fraction (Steele et al., 1989; Martinson and Wamser, 1990; Worby and Allison, 1991; Andreas et al., 1993; Martinson and Iannuzzi, 1998; Bigdeli et al., 2018; Castellani et al., 2018; Gupta et al., 2020).
Due to the lack of better observational constraints, changes in remotely sensed SIC over a range of timescales should still be used as the main indicator of responses to the environmental drivers. In the following, I will refer to these features and drivers as the “MIZ characteristics”, even if they occur in areas that are distant from the sea ice edge. The atmospheric and oceanic drivers that are more active in these regions modify the sea ice area and extent and should not be considered absent in regions with 100 % cover. There is growing evidence in the Southern Ocean that (1) extended regions with mixed types of sea ice in a fully covered ocean show MIZ characteristics from austral winter to spring (Alberello et al., 2019; Vichi et al., 2019; Alberello et al., 2020; Womack et al., 2022), (2) waves penetrate deep into the pack ice throughout the seasons (Kohout et al., 2014, 2015; Stopa et al., 2018; Massom et al., 2018; Kohout et al., 2020), and (3) extended regions of high variability in sea ice concentration and drift can be found in correspondence to large-scale synoptic events (Vichi et al., 2019; de Jager and Vichi, 2022). Figure 1 gives an example of the complex conditions observed in the Antarctic MIZ. The synthetic aperture radar (SAR) image shows a pattern of the MIZ in austral spring that is very well captured in the AMSR2 data, which report 100 % concentration very close to the edge where the ship was located (Fig. 1b). The ice-covered ocean was confirmed, but the sea ice type was classified as grey-white ice, with a combination of thin fragments and frazil ice from refreezing (Fig. 1c). These conditions extended southwards throughout the area of 100 % cover. Also in regions of cemented pancakes as shown in Fig. 1d, waves associated with intense extratropical cyclones can penetrate and modify the surface features extensively (Vichi et al., 2019). Finally, we should also note the confounding effect of building composites from satellite swaths, with a clear discontinuity line in the SIC field between 3–5∘ E in Fig. 1b that is indicative of substantial sub-daily changes in the sea ice cover. A threshold-based indicator of MIZ characteristics may thus lead to erroneous definitions of sea-ice characteristics and their parameterisation in models, with unpredictable consequences for the design of observational campaigns and model predictions.
1.3 The need for a novel indicator
The growing body of observations poses the problem of having a proper description of the Antarctic MIZ and of Antarctic sea ice variability in general. Every latitude of the Southern Ocean, apart from the few regions of multi-year ice, can be classified as seasonal sea ice zone. This implies that for a period of time of variable duration, the sea ice may present MIZ characteristics, which may not necessarily be found at the margin of the ice-covered region. In this work I reassess the assumption that absolute thresholds of SIC contain sufficient information to characterise Antarctic sea ice, in contrast with the Arctic, where a better correspondence between ice cover fraction and ice type allows the discrimination of first-year (seasonal) ice from multi-year ice, with the subsequent emergence of categories based on thickness and ice age. This is less relevant in the Antarctic, where the majority of sea ice is thin and seasonal. Antarctic sea ice and its MIZ features cannot thus be decomposed into further categories, unless through direct observations or the use of high-resolution SAR images, which are limited in space and time. Given that the only available data at the planetary scale are passive microwave data of brightness temperature, there is merit in investigating whether smaller changes in pixel concentration from remote sensing hold some consistent measure of change in the ice character.
In the following sections, I will demonstrate how the use of an indicator based on the SIC standard deviation of daily anomalies computed over the monthly timescales allows the reconciliation of the mismatch observed in the seasonality of the MIZ extent in the Antarctic when using different satellite products. This indicator is meant to quantify the temporal variability in SIC over each month, and I will compare its magnitude against the spatial variability to show that time variability is an intrinsic feature of the MIZ. This variability combines together the advance–retreat of sea ice within a month, as well as the daily changes in SIC caused by the passage of storms (e.g. Vichi et al., 2019). I will then investigate sub-seasonal-scale variability in SIC with the aim to construct climatological maps of MIZ features in Antarctic sea ice, as complementary information to the threshold-based classification. The interest here is not whether the retrieval of brightness temperature is measuring the actual concentration of ice-free versus ice-covered ocean but rather if the relative time change in this proxy is representative of a physical variation in the sea ice state. In this first work, I will not link the observed variability to the possible drivers, but I will present the advantages of this method with respect to the threshold-based MIZ definition. Further analyses can be performed eventually based on this rationale. In the following, the indicator will also be used to construct climatological maps of SIC variability and the probability of exceeding extreme values of variability, hence assisting with long-term navigation planning, design of observational experiments and assessment of model outputs.
2.1 Remote-sensing data
The analysis was carried out using SIC data from the sea ice Climate Data Record (CDR) from NOAA/NSIDC (Peng et al., 2013; Meier et al., 2021, version 3 and 4) and from the EUMETSAT OSI SAF (OSI-450) product (Lavergne et al., 2019). The two datasets were initially chosen for their different approaches. The NOAA/NSIDC CDR until version 3 (Meier et al., 2017) represented a level-3 product that followed all the standards for traceability and reproducibility with minimal filtering; since version 4 it has been a level-4 product, with additional gap-filling procedures that have been introduced to make the estimates of sea ice extent (SIE) more comparable with other products (Windnagel et al., 2021). The OSI-450 product is a gapless, level-4 product, which includes additional manual corrections and spatial–temporal interpolations to fill data gaps. The data processing of OSI-450 also used an open-water filter aimed at removing weather-induced false ice over open water, which may also remove some true low-concentration ice in the MIZ (Lavergne et al., 2019). OSI-450 provides a variable containing the raw data, which has been used to further assess sea ice variability.
The NOAA/NSIDC CDR product is meant to be an improvement on the individual algorithms, namely the NASA Team (NT) and the bootstrap (BT). The rationale behind this choice is that passive microwave algorithms tend to underestimate concentration during the summer melt season (Meier et al., 2014). Since greater underestimation is typical in the BT algorithm, the CDR implements a 10 % cut-off of this field and maximises the values between the two above the threshold. This means that all values lower than 10 % from the BT product are not included in the CDR. As indicated in Sect. 1.1, the NT and BT algorithms have shown major differences when estimating the MIZ extent and its seasonality (Stroeve et al., 2016). The CDR will then be compared against the individual products because the rationale for its construction does have an impact on the MIZ estimation.
For the purpose of this analysis that focused on daily variability, NOAA/NSIDC CDR version 3 was preferred for the lower level of smoothing and aliasing, which highlighted conspicuous features of the MIZ. With the new version 4 and likely future versions, the NOAA/NSIDC CDR has implemented the spatial and temporal filtering which in version 3 was only applied to the Goddard merged product that extended the period back to January 1979. The NOAA/NSIDC CDR has practically substituted the Goddard merged product, and it is more similar to the OSI-450 in terms of large-scale properties. To reproduce the results observed in version 3 (not available online anymore), the analysis has been performed on a reprocessed version, which corrects some bugs in version 4; removes the interpolated pixels; and focuses on the period 1987–2019, for which daily data are mostly available. The scripts for this processing are available in the Supplement. In the following, the results will be discussed against the other datasets, and the corresponding figures for NOAA/NSIDC CDR version 3 and OSI-450 CDR are available in the Supplement.
2.2 Statistical analysis of variability
The methodology treats the variability in remotely sensed SIC as if it were a perturbation around an expected value. In the following, SIC is expressed as the fraction between 0 and 1; this value is assumed to be an objective measure of the sea ice state rather than an actual indicator of ocean coverage. Regions of closed pack ice or of ice-free ocean outside the seasonal ice zone are more likely to experience small variations around a long-term mean value of the SIC (close to 1 in the former case and to 0 in the latter). Persistent conditions of multi-year ice and permanently ice-free ocean will have less noise, hence a negligible dispersion around the climatological mean. The standard deviation of the daily SIC anomaly with respect to a chosen reference value can thus be used to measure the degree of variance in sea ice conditions experienced by a certain pixel over a month.
The daily SIC anomaly for each pixel is computed by subtracting the daily SIC from the monthly climatology :
where the index i runs over the number of days in month m and indicates the month of the year. The index m runs over the total number of months in the time series (e.g. 396 for NOAA/NSIDC CDR). The reason for choosing the monthly climatology as the reference value is crucial for the analysis and further explained below. Since the variable SIC is constrained between 0 and 1, so is the anomaly. The standard deviation of the daily anomaly is then computed for each month to measure the spread around the climatological SIC monthly mean as follows:
where N is the total number of days in the month. The standard deviation is effectively a sum of squares, since the mean of the anomalies is null. The climatological monthly standard deviation of the anomalies has also been computed by pooling together all the daily anomalies from the same month in different years:
with Y being the number of years and the index j running over the number of days of the Januaries, Februaries, etc. The variable , hereinafter referred to as “the indicator” σSIA with the index m dropped, describes a left-bounded distribution, where the value 0 indicates lack of SIC variability over the month and the maximum expected value is 0.5. The exclusion of the zeroes represents an unbiased distribution of SIC variability.
This analysis does not deliberately discriminate between a point that is experiencing a seasonal transition of the MIZ band during sea ice advance or a persistence of short-term variable SIC conditions more typically ascribed to the ice edge. This is the main reason for using the daily anomaly against the monthly climatology instead of the daily climatology (based on daily values or daily running means over a weekly to monthly time window). The use of a filtered background climatology with a window shorter than a month would include the smooth daily transition during the advance and retreat phase. It does retain some measure of variability but reduces the variance of the signal due to the meridional advancement, which is a fundamental characteristics of the MIZ. On the other hand, this same analysis conducted over the weekly scale would enhance the role of synoptic forcing. The method chosen here encompasses both aspects. Since the anomaly is computed roughly over the same number of days for each pixel (excluding the random missing data), it is more likely that a rapid transition between new, young and first-year ice would result in an overall lower value of the monthly indicator, nevertheless recording the information that this region of the ocean has been partly affected by small changes in SIC.
The difference between the temporal variability expressed by this index and the spatial variability has been analysed by comparing it with the NOAA/NSIDC
stdev_of_cdr_seaice_conc, which computes the spatial standard deviation of the box of 9 pixels surrounding each
pixel. This measure takes into account the uncertainty in an SIC value based on the variability in the adjacent pixels. I used the monthly average of
the latter, and I assumed that the σSIA indicator is a valid measure of temporal variability, indicative of MIZ conditions when the
ratio with the spatial variability is smaller than 1.
The indicator is finally used to estimate the chances of encountering variable MIZ conditions at each pixel on a monthly climatological timescale. The probability of an ocean region being affected by MIZ conditions during a given month has been computed using the empirical exceedance (which is equivalent to 1 − CDF, the cumulative density function, when the function is known):
where r is the rank of the sorted series of values. Given a certain threshold of the indicator that is known to correspond to MIZ conditions, this function gives an empirical estimate of the probability of exceeding that value.
3.1 An indicator of climatological variability for the MIZ
The empirical distribution of σSIA follows a Pareto distribution (Fig. 2). In a Pareto distribution, the median is biased towards the lower values, indicating a majority of pixels with low SIC variability, but the tail of the distribution is sufficiently fat to have an influence. The cumulative density function is a power law, which can be fitted well with the Pareto function (p value of the Kolmogorov–Smirnov test is virtually zero; the test had to be run on sub-samples for computational reasons). The empirical function slightly departs from the fitted distribution for values above 0.1, which could be indicative of the superposition of two distributions.
Since the interest is in identifying the typical conditions differentiating the MIZ pixels from those belonging to consolidated and less variable SIC regions, the median of the indicator computed for each pixel is a useful descriptor for obtaining a map of spatial features (Fig. 3a). Higher values of the σSIA median are indicative of larger departures from the long-term conditions (when sea ice is present in the region). These highly variable regions are found in the outer part of the sea ice as expected. They are distributed zonally in a rather homogeneous way, with a few peaks in the Bellingshausen, eastern Weddell Sea (13∘ E) and Ross Sea (150∘ W) regions, located close to areas of interruptions of the zonal belt. Another area of high median values is associated with coastal polynyas. These are known regions in which the SIC is recognised to be more variable and usually less consolidated. A greater halo of scattered variability is observed mostly in the Atlantic and East Antarctic sectors, extending to about 55∘ S. This halo is removed when the analysis is run on the unprocessed CDR (see Sect. 2.1 for more details) and OSI-450, which are gapless and/or filtered, and it is enhanced in NOAA/NSIDC CDR V3 (Figs. S1 and S2 in the Supplement).
The median distribution shown in Fig. 3b confirms the presence of different processes underlying the variability in Antarctic SIC. The distribution of the σSIA median is more log-normal and bimodal than the overall sample distribution presented in Fig. 2, with maximum values below 0.3 (0.2 is the 99th percentile). There is still a large percentage of values with very low intraseasonal variability (which was not found in V3; see Fig. S2), but the bimodality is evident. The first peak is larger and centred around 0.03, and the second one is above 0.15, with a trough between 0.1 and 0.15. The change in slope in the empirical CDF is more evident here and corresponds to the range of values where the two distributions presumably intersect. By combining the spatial map with the distribution of the median, we can say that values between 0.1 and 0.15 indicate mixed regions where consolidated pack ice may show concentration changes akin to the features observed at the ice margin, and values above 0.15 can be clearly identified as having MIZ-like features.
The same analysis performed for the Arctic (Fig. 3c and d) indicates that the regions of higher temporal variability in SIC at the sub-seasonal scale are narrow and confined to the Bering, Greenland, Irminger and Norwegian Sea areas, as reported in the literature (Wadhams, 2000). The empirical distribution of the median is also different from that of the Antarctic. The number of pixels with low variability is larger, as is known to be the case in the Arctic due to the presence of multi-year ice, and the second peak is lower and barely visible. There is instead a plateau of points that show median values of the indicator between 0.05 and 0.17, and a clear threshold is less distinguishable.
In the following I will only focus on Antarctic sea ice, and I will use the 0.1 threshold as the lower limit of the trough in Fig. 3b. The results are insensitive for a 20 % variation around this value, and I will discuss the implications of this choice in Sect. 4. Note that this analysis does not differentiate regions of high temporal variability based on the distance from the continent, as for instance done in Stroeve et al. (2016) with the SIC-threshold criteria. Regions of high temporal variability showing MIZ-like conditions can also be found in the interior of the sea ice, as will be further analysed in Sect. 3.3. It is remarkable to note that the heavier filtering and gap filling used in the standard NOAA/NSIDC CDR version 4 and OSI-450 introduce a smoothing in the distribution of the median that flattens the second peak and removes much of the variability in the MIZ (Figs. S1 and S2).
The NOAA/NSIDC CDR computed in Eq. (3) is shown in Fig. 4 as an overall climatological indicator of SIC variability in the Southern Ocean. The standard NOAA/NSIDC version 4 and OSI-450 are substantially equivalent but with less noise associated with values lower than 0.1 in the open-ocean region (see Fig. S3 in the Supplement; the OSI-450 product also leads to slightly smaller values of the σSIA climatology at the ice edge because of the use of a stronger open-ocean filter). The extent of the regions presenting MIZ features increases from November to December in a diffused fashion. Later in the austral winter season, these regions are confined within a band around the sea ice edge that progresses northwards and shrinks at the boundary with the ocean. The higher values and the largest meridional spread are found in April and May in the Weddell and Ross seas. In June and July, the large expanse of the eastern Weddell Sea between 15∘ W and 40∘ E corresponding to the Atlantic bulge of the sea ice edge is characterised by large SIC variability that extends towards the continent. The value of the indicator can also be appreciated by looking at how it captures the variability corresponding to the Maud Rise polynya. The impact on SIC variability in this area is visible from September and throughout November, with the latter characterised by a climatological value above 0.2 over a large expanse of the sea-ice-covered region. In November, this region denotes a decrease in the indicator because the polynya is usually fully developed and the open-ocean traits prevail.
3.2 Assessment and regional analysis
The climatological maps are useful to highlight the seasonal features of the MIZ, which will be further analysed in the next section. However, it is relevant to first appreciate the uncertainty associated with the assumptions of the indicator and analyse how it differs from the more traditional analysis based on the operational SIC threshold. One of the assumptions is that MIZ conditions are more evident as temporal changes over the monthly scale at any given observable point. Antarctic sea ice is highly variable at a variety of scales, and this variability can be distinguished in terms of temporal variability at a given location and spatial variability over a certain region. An ergodic process is characterised by its time mean being equal to the ensemble (spatial) mean over a given temporal and spatial ambit. In an ergodic process, space and time variations are interchangeable. Sea ice can be modelled like an ergodic process (Hogg et al., 2020), and this assumption is also made when detecting variability from multi-model ensembles (e.g. Horvat, 2021). The Antarctic MIZ is however largely under-sampled, and there is limited knowledge on whether time variability and space variability are equivalent. To check if σSIA is an indicator of physical variability in the sea ice, I have compared it with the estimated spatial uncertainty from the NSIDC/NOAA CDR (Sect. 2.2). The mean climatological values for the months of December and August are shown in Fig. 5a and b, chosen as examples of austral summer and winter months before the months of minimum and maximum extent. In summer, the mean spatial standard deviation of the sea ice cover fraction is below 0.1 almost everywhere except in the regions of coastal polynyas. In winter, the highest spatial variability is found at the edge, corresponding to the MIZ region. Figure 5c and d show the ratio between the spatial variability and the indicator from Fig. 4. This ratio is lower than 1, in the range 0.1–0.3, for the large majority of the ice-covered ocean, besides the pack ice region in August. Mean temporal variability thus exceeds spatial variability in the MIZ region in winter, also hinting at a dominance of local temporal variability in the extended summer MIZ. I also notice that the standard deviation of the anomaly used in the definition of σSIA is a lower-range estimate of variability, since it captures the inter-annual component. The same analysis performed on the spatial standard deviation would likely lead to smaller values, further lowering the ratio in the MIZ regions. This relationship holds for all the other months, as shown in Fig. S4.
A main question is whether the proposed indicator performs “better” than the operational definition of the MIZ. I argue that this question cannot be adequately answered for two main reasons: (1) the use of a threshold-based MIZ has not been objectively assessed in the literature but merely applied operationally, which poses a considerable challenge when proposing any alternative indicator; (2) there are no ancillary observational datasets (at least not derived from passive microwave measurements) that would allow an independent assessment of any metrics. MIZ diagnostics are usually applied in climatological or integrated analyses (for shorter times and specific regions, SIC is the variable of preference), and as such it is difficult to assess them against local ship observations or SAR images. However, these points should not dissuade us from comparing them with data that have sufficient time coverage, for instance buoy data lasting longer than a month, or comparing the different metrics without a benchmark, as typically done in model intercomparisons projects.
I offer two examples to demonstrate the advantages of this diagnostic. Womack et al. (2022) analysed the trajectory of an ice-tethered, non-floating buoy that drifted through the marginal zone in the East Antarctic sector for more than 5 months from July to the beginning of December 2017. The study indicated that the sea ice was permanently in free-drift conditions with SIC close to 100 %, showing a high correlation between the sea ice drift and the wind direction, as well as various loops in the trajectory in correspondence with the passage of extratropical cyclones. The paper focused on the daily changes in SIC and the buoy distance from the edge. In this example I compare the pathway of the drifter over each month against the average monthly location of the threshold-based MIZ location and the map obtained with the σSIA indicator. We observe that in winter there is good correspondence between the two diagnostics, as further shown in Sect. 3.3 and Fig. 10, but the shaded field indicates that SIC has been more variable in the interior of the sea ice where the buoy drifted, as well as in the outer edge in December when the buoy sank. The MIZ was not homogeneous in July and August, and although this variability did not show in the SIC values at the buoy location, the spots of high σSIA values indicate the presence of synoptic activity at the margin (Vichi et al., 2019; Womack et al., 2022) that resemble the trajectory of the buoy. September and October were quieter, although we still observe high intensity at the margin that coincides with the meandering of the trajectory. Such details cannot be obtained with the analysis of the MIZ contours alone because it is difficult to trust a bending of the 0.80 contour level, while the confidence increases when it is associated with consistent areas of intense variability.
As a further example of intercomparison with the operational MIZ definition, Fig. 7 shows that the proposed indicator is sensitive to inter-annual variability in months that have been reported as anomalous, and there are more details than can be derived from the threshold-based MIZ. November 2016 was very anomalous with respect to the previous years in terms of SIE (Turner et al., 2017; Parkinson, 2019), and this has been captured in the threshold-based MIZ extent (shaded region in Fig. 7a). However, looking at the same year in Fig. 7b, the whole Atlantic sector was characterised by intense and extended MIZ-like conditions, not only in the region of the Maud Rise as indicated by the SIC thresholds in Fig. 7a, a condition that persisted until 2019. The threshold-based MIZ definition only indicates the extent and not an intensity of the MIZ conditions, although values below 0.8 are indicative of gaps in the cover that persisted for a month. According to the indicator, there was also large temporal variability at the boundary between the Amundsen–Bellingshausen and the Ross Sea sectors, which is not visible in Fig. 7a. In addition, Novembers 2017 and 2018 were not much different from the earlier years before 2016 in terms of the mean SIC apart from the Maud Rise polynya in 2017, while the σSIA analysis highlights a persistence of large temporal variability in the Atlantic sector. Similar conditions were previously observed in 2009–2010 (see Figs. S5 and S6), which was another period of negative SIE anomalies especially recorded in the Weddell Sea and Indian Ocean regions (Parkinson, 2019, their Figs. 3 and 4).
I have also tested if sectors with more extended sea ice are more prone to temporally variable SIC and thus exhibit covariance with large σSIA values. The MIZ fraction has a complex regional relationship with the SIE, with a seasonal cycle that differs for different Antarctic regions (Stroeve et al., 2016). The sectors have been defined following Raphael and Hobbs (2014), since they proposed a separation based on large-scale atmospheric drivers rather than using arbitrary longitudinal boundaries. The total maximum monthly SIE for each sector and each year in the period 1987–2019 has been plotted against the MIZ SIE computed with the 0.15–0.80 threshold and analysed in combination with the value of , averaged over the sector and the whole year (Fig. 8a and b). This latter diagnostic gives an indication of the mean variability in the MIZ in each sector, and it can be done this way because the minimum and maximum extents fall within the same calendar year in the Antarctic sea ice season.
The various sectors show quite distinct clusters, with only some overlap. If we consider all sectors as a single cloud of points, both the minima and the maxima of the MIZ extent follow a linear relationship with the total SIE (Fig. 8a and d). The Weddell Sea (WS) shows the largest SIE in summer with the largest inter-annual variability, and the points cluster around the 25 % line. The MIZ fraction is higher in the King Haakon VII (KH) sector, around 50 %, and in the Amundsen–Bellingshausen (AB) sectors, while the Ross Sea (RS) and East Antarctica (EA) have an intermediate minimum SIE, with an MIZ fraction larger than 50 %. We observe a decreasing trend of MIZ variability with the increasing SIE in summer: the sectors with low SIE like KH and AB also have a highly variable SIC, indicated by the higher values of σSIA. The EA sector does not follow the linear trend because the variability is lower than in the other regions. The SIE here is comparable to the WS during summer, but SIC departs less from the mean monthly climatology. Since the seasonal cycles are different in each sector, the clustering of the maxima shown in Fig. 8d is not the same as in Fig. 8a, and also the spread of different years is lower. During the maximum winter SIE, we note that regions with different magnitudes of SIE and different MIZ fractions have the same amount of variability. The AB, RS and KH sectors have similar ranges of the mean σSIA, although the Weddell Sea records the highest values. In general, the magnitude of SIC variability appears to be independent of the characteristics of the sectors. Only the East Antarctic sector still stands out as the region in which the MIZ fraction is extended in winter but with relatively lower intrinsic SIC variability than in the other sectors. The estimate of the MIZ extent based on counting the area of pixels with has also been computed and shown in Fig. 8c. This will be discussed in the next section together with the climatological seasonal cycle of the whole Antarctic MIZ.
3.3 Patterns of seasonal variability
The above analysis highlights that, due to the intrinsic seasonal nature of Antarctic sea ice, there are wide regions where SIC shows high inter-annual variability in every month of the year, which is only partly captured by analysing the mean monthly concentration. To strengthen this concept, the seasonal cycle of the circumpolar MIZ extent was computed from the monthly indicator for every year and then averaged. This measure is comparable to using the mean monthly SIC of between 0.15 and 0.80 to compute the extent. Following from the results shown in Sect. 3.1, any pixel with a value of the indicator larger than 0.1 was assumed to be characterised by MIZ processes and included in the spatial integral. Figure 9 shows the comparison between the MIZ extent computed using the 0.15–0.80 SIC criterion and the one proposed here, for all the products described in Sect. 2.1. As previously shown by Stroeve et al. (2016), the MIZ area based on the SIC threshold is largely affected by the retrieval algorithm. In their analysis, the NT algorithm had a higher MIZ area than BT and a larger proportion of inner open-water ice and coastal polynyas, which are included in this MIZ threshold-based criterion, and hence the absolute value shown here is higher than the one presented in Stroeve et al. (2016, their Fig. 5). The σSIA-based MIZ extent is instead independent of the algorithm choice or product because the relative variability is equally captured. We notice that in the NOAA/NSIDC V4 product the BT and CDR estimates are very similar (Fig. 9a), while the threshold-based estimate of the MIZ extent computed with the CDR from V3 was much lower (Fig. S7 in the Supplement). The threshold-based MIZ seasonality (Fig. 9a) grows linearly from summer to spring, when it increases sharply until the peak in December. The inter-annual spread indicated by the shaded area is similar throughout the year, apart from the NT product that increases in winter and spring. The cycle obtained from the σSIA indicator shows a greater increase from February to May, and then the MIZ extent remains constant but more variable from year to year. This alignment of the BT and NT products is not a result of the climatological averaging, as shown in Fig. S8 in the Supplement. We also note that in the anomalous 2016, the progression of the MIZ extent was more linear and similar to the threshold-based climatology. The November MIZ extent was still in the range of the previous years, while it collapsed in December.
This indicator quantifies the intensity of temporally variable MIZ conditions, as opposed to the SIC range criterion, which returns a binary mask based on the average concentration. A climatological MIZ mask can still be obtained by considering the pixels that are climatologically more likely to present MIZ features (with values of , Fig. 10). Here we observe that the two criteria are more similar in the winter to early spring months from July to October. However, the MIZ mask is generally wider and more extended both onto the open ocean and into the pack ice. This is more evident in the eastern Weddell Sea from 0–50∘ E and also in the Ross Sea between 120–160∘ W. This difference increases from October to June, with a peak in November. The latter is indeed the month that has shown the largest variability in the records (Turner et al., 2017), as previously highlighted in Fig. 7. This increase in the MIZ extent is also visible in the regional analysis of the minimum and maximum MIZ extent obtained with the same method and shown in Fig. 8c and f. In the month of minimum extent (February), all sectors show a higher fraction of pixels with MIZ features, with the MIZ fraction also exceeding 100 %. There is also more year-to-year variability in the Weddell Sea MIZ extent than with the SIC range criterion (Fig. 8a). However, the relationship between the sectors is unchanged. It should not be surprising that the MIZ extent presented in this work exceeds the total SIE. This is because this method detects pixels that are statistically more likely to be affected by changes in SIC from year to year, rather than the pixels that had an average monthly mean of SIC > 0.15. Antarctic sea ice can drift quickly in a short period of time and for a few days over a month. This would temporally change the concentration, but it is less likely to affect the mean variability unless these changes occur several times. This indicator has been specifically designed to capture this property and to give a likelihood of encountering MIZ conditions, as will be presented in the next section.
There is finally a fundamental computational difference between the climatological averaging of the monthly extents shown in Fig. 9b, in which a monthly mask is multiplied by the pixel area and then integrated over space and averaged over the years, and the mask based on the climatological monthly standard deviation of the daily anomalies . This is because the average of the standard deviations computed from sub-samples of a population is different from the standard deviation of the whole population. Note that this difference also applies to the computation of the extent using the SIC range criterion. Hence, the climatological MIZ extent shown in Fig. 9 is an underestimation of the sea ice area that may statistically present MIZ characteristics. This is graphically shown in Fig. 11, where the climatological sea ice extent (SIE) is computed from the SIC criterion and indicator (the area of the yellow-shaded region in Fig. 10) using the NOAA/NSIDC CDR. The MIZ SIE obtained with the climatological SIC criterion (the line with the crosses) is also higher than the one shown in Fig. 9a (compare with the blue line obtained from the same product).
3.4 Exceedance probability of encountering MIZ conditions
The previous analysis revealed that MIZ-like features in Antarctic sea ice are not necessarily confined to the outer edge or to coastal polynyas but can also extend to the interior of the pack ice. It is therefore of interest to quantify the likelihood of encountering MIZ conditions in a selected month. The probability of exceeding a given value of variability according to the method presented in Sect. 2.2 is shown for the substantial threshold σSIA>0.2 in Fig. 12 (the maps for the σSIA>0.1 are shown in Fig. S9 in the Supplement). The presented value is twice the threshold used in the previous sections to assess the probability of encountering extremely variable sea ice states (σSIA=0.2 is the 99th percentile of the distribution of medians shown in Fig. 3).
The exceedance probability is different from month to month in different sectors of the Southern Ocean (Fig. 12). This is consistent with the lack of consistency when comparing regional and hemispheric values of SIE trends. For instance, the Ross Sea presents the highest chance of finding a variable sea ice state in March over the entire region, while in December this is more likely in the Weddell Sea and in the Indian Ocean sector up to 90∘ E. The regions where the extent of sea ice from the continent is narrower, such as East Antarctica, tend to show less variability in the sea ice state. In more accurate terms, the probability of exceeding a high value of the indicator in East Antarctica sea ice is lower with respect to the other regions, but the whole sea-ice-covered region should be classified as MIZ, since the probability of exceeding the 0.1 threshold is above 80 % in every month (Fig. S9). This region is therefore one of the most interesting to capture the seasonal processes at the air–sea ice–ocean interface because the MIZ remains confined within the same latitudinal band throughout the year. Combining this information with the analysis presented in Fig. 8, we may conclude that there is lower year-to-year intensity of variability in East Antarctica (in terms of the magnitude of the anomalies) but that the sea ice state is in a permanent MIZ condition.
In general, there are lower chances of exceeding the threshold value both on the outer edge and in the internal pack ice. This feature is caused by two different processes. At higher latitudes (mostly in autumn and winter), it is less likely we will find variable conditions because the sea ice advances so far north only in a few years. February is an interesting month because in almost every pixel in which sea ice has been observed in the satellite records there is a similarly low probability of exceeding the threshold. This means that there are small chances of encountering brash ice but it is more likely that open-drift conditions will be prevailing. At lower latitudes, on the other hand, the probability is close to zero is because there are persistent pack ice or polynya conditions (the white regions between the coloured sectors and the Antarctic continent). They can be found in all months but March, which only shows the few regions of multi-year ice in the eastern Weddell Sea and the Ross Sea polynya. These are regions where consolidated conditions and sea ice features that are more likely to be similar to the Arctic are found according to the satellite records.
June and July are instead the months of higher chances of encountering SIC variability away from the edge towards the interior of the eastern Weddell Sea and hence a sea ice state that is more typical of the MIZ. In these regions, assuming pack ice conditions in numerical models and other conceptual considerations may lead to an underestimation of the air–sea exchanges. The SIC values may be generally close to 100 %, but the fluctuations around this value are large, which is indicative of a sea ice state that is affected by boundary processes.
4.1 Towards a multivariate definition of the MIZ
This work aims at reviewing the way we consider the Antarctic MIZ, shifting the perspective from considerations based on the absolute concentration to the relative temporal variability. This is seen as one way to overcome the difficulties of detecting a clear relationship between concentration and ice type in the Southern Ocean. The MIZ should be defined in terms of the physical processes that shape the type of ice and its stages of formation and decay, from pancakes to grey-white ice to young and first-year ice. Unfortunately these properties cannot be derived at relatively high frequency and large scales; therefore SIC from space should be further exploited to give insights into the variability in Antarctic sea ice instead of just its mean state. The use of absolute SIC thresholds does not tell the whole story of the MIZ seasonal cycle, and especially it does not give a direct measure of the temporal variability, which I demonstrated to be a characteristic that dominates over the spatial variability in the MIZ (Fig. 5).
The proposed method is complementary and extends the traditional threshold-based definition, hinting at the importance of using a multivariate approach for the MIZ definition that combines mean and variance. It allows the identification of regions of higher variability and quantification of the climatological relative intensity. It gives a quantitative measure of the sub-seasonal variation in SIC and not only a binary map as can be obtained with the threshold-based MIZ definition. The method is derived from the standard deviation of the daily anomaly with respect to a monthly climatology, a common diagnostic in the climate sciences. This indicator can be translated into maps of exceedance probability, hence giving a quantitative description of the likelihood of finding MIZ characteristics. The method does not require a priori ranges because the separation between pixels of low and high variability is obtained through a distributional analysis that reveals a bimodal pattern in the Antarctic.
A threshold is nevertheless necessary, which is defined as the trough that distinguishes points of low variability, which are more typical of the inner pack regions, from the more variable MIZ regions. This implies that conditions of high variability similar to the ones found at the margin can also be found in more consolidated sea ice regions from a climatological viewpoint, in agreement with the observed penetration of waves deep into the pack ice (Kohout et al., 2014, 2015; Stopa et al., 2018; Massom et al., 2018; Vichi et al., 2019; Kohout et al., 2020). Whether this variability has to be attributed to the incidence of extratropical cyclones that stimulates daily SIC changes is currently being investigated. Intense cyclones have a systematic statistical association with atmospheric temperature extremes over Antarctic sea ice (Hepworth et al., 2022). However, the same study reports that moisture extremes are more associated with atmospheric rivers at the sea ice margin, and there is still a large portion of extreme atmospheric events in the interior of the pack ice that cannot be related to the presence of cyclones. Whether extreme atmospheric events are needed to engender variability in the pack ice that persists at the climatological scale is still an open question, and this same indicator can be applied in this context by considering anomalies over the synoptic timescales.
One main concept of the methodology presented in this work is the use of daily SIC anomalies derived from the climatological monthly mean. This is based on the evidence that Antarctic sea ice has a clear seasonal pattern (Eayrs et al., 2019) but high variability from year to year and uncertain trends in different regions (Matear et al., 2015; Yuan et al., 2017; Parkinson, 2019). I remark that this indicator is explicitly constructed to combine the sub-seasonal variability due to the advancement and retreat of sea ice, as well as the smaller-scale changes in response to the synoptic weather, such as the passage of extratropical cyclones. Regions with higher mean variability like the King Haakon VII sector (Fig. 8) are indeed those with the higher incidence of extratropical cyclones and where sea ice trends are likely driven by the weather (Matear et al., 2015; Vichi et al., 2019). The same indicator has been applied to the Arctic, where the ice cover fraction is used as an indicator of the ice type. The analysis of the distribution median shows a much larger density of pixels with low temporal variability (multi-year and thicker pack ice) and a less extended tail with higher SIC variability. This confirms that SIC has smaller sub-seasonal variability than in the Antarctic, and the use of the threshold-based definition is likely sufficient to capture the regions where MIZ processes occur. Nonetheless, this indicator could be useful in studying transitional seasons and could be applied to different periods to assess whether there has been an increase in sub-seasonal variability with the increased Arctic sea ice loss.
The results presented in Fig. 9 have shown that this indicator removes the mismatch in the estimation of Antarctic MIZ extent using different algorithms (Stroeve et al., 2016). The CDR and the BT NOAA/NSIDC threshold-based estimates cluster together with the OSI-450 product, while NT is much larger. This was not the case with NOAA/NSIDC V3 (Fig. S7a). This mismatch is not visible with the σSIA estimates, which indicates that the threshold-based definition is sensitive to the specific data processing, while the variability captured by each data product remains the same.
4.2 Caveats and future applications
A note of caution is necessary to clarify the difference between the MIZ extent derived with the 0.15–0.80 range and the climatological mask obtained through the σSIA indicator (Fig. 10), as well as the related seasonal cycle (Fig. 11). This masking method (where pixels with σSIA>0.1 are classified as MIZ points) is complementary to the MIZ SIE and should not be used for computing the marginal ice zone fraction (like in Horvat, 2021). The SIE criterion must be the same for both the MIZ and the total ice cover. However, the study of the MIZ fraction may be less sensitive in the Antarctic, and a comparison between model outputs and satellite data using this indicator may give interesting insights. There is no incongruence in the mismatch between these estimates of the MIZ extent because they measure different properties. In terms of the seasonal climatology, the MIZ area obtained through the use of a fixed threshold slowly grows in winter and is below the total summer area (Fig. 11). The estimated MIZ area using the indicator reaches a plateau during the austral winter months and is instead more extended in summer than the total SIE. This may seem paradoxical because the region classified as MIZ cannot be larger than the sea ice extent. This is however an artefact of the use of climatological means and the 15 % baseline, which skews the distribution towards the low values, disregarding the natural large variability in Antarctic sea ice and the diversity of ice types. There are more pixels where daily SIC anomalies have values larger than 0.1 at the sub-seasonal scale in summer. This also includes the polynya regions, which, due to their nature, are more affected by daily changes in weather conditions. The proposed analysis is therefore more oriented towards the estimation of variability due to heterogeneous ice conditions, independently of where they are located.
There is no specific reason that the proposed indicator is the best method to quantify the variability. Alternative indicators could be used, such as the monthly averaging of daily maps of the SIC-threshold MIZ (i.e. identified points with 0 every day) instead of defining the threshold based on the monthly climatology and hence a monthly mask. This method would indeed add a measure of intensity but would still not detect changes when sea ice is above 0.80, a condition often found in the MIZ. This does not mean that the threshold-based estimates are not accurate but that there are regions of the ice-covered ocean that present physical characteristics similar to the MIZ even when the SIC fraction is above 0.80. Perhaps, as shown by the buoy example presented in Fig. 6, it is in the regions around the 0.80 SIC level that most of the missed variability is found. However, the drift data indicate high mobility in areas where σSIA is still not high enough, which indicates that this variability is probably more active at the synoptic timescales.
To conclude this discussion, I would like to offer a critical analysis on the use of SIC products that have been optimised for climate studies, like the CDR presented in this work. SIE, as an essential climate diagnostic, has been designed to be a smooth measure of long-term climatic variability. My perspective is focused on Antarctic applications, which are less likely to be supported by direct observations, and methodologies developed for the Arctic tend to be used in Antarctica with a necessarily limited validation. The same method proposed here is indeed supported by a few examples only because a more systematic analysis is not yet possible. Users may not always be aware of the subtleties of the satellite-derived products. For instance, the differences between NOAA/NSIDC CDR V3 and V4 are substantial, as shown in the figures in the Supplement. The choices of filling gaps and enhancing the similarity with other products (Windnagel et al., 2021) are very legitimate, but users may imply that these products and versions are interchangeable. A variety of derived products should then be made available to the users, as proposed by Lavergne et al. (2022), to allow for different types of analyses. On the other hand, it is known that SIC from space is prone to major assumptions and corrections because the algorithm often exceeds the unit fraction and it is truncated to 1 (Kern et al., 2019). This has implications for the analysis of variability carried out here. Some variability may be dampened by the filters or even enhanced, especially when spurious values close to 0 are not eliminated. SIC from space is the result of an empirical model applied to selected bands of the passive microwave spectrum with few tie points, and as such it cannot encompass all the ice types found in the polar ocean. In addition, day-to-day variability is biased by the construction of composites of different swaths to obtain a daily picture of the sea ice distribution. As suggested by Kern et al. (2019), the use of non-truncated datasets would enhance the analysis of variability. However, estimates of threshold-based MIZ extent using these datasets are not yet available in the literature, and this application goes beyond the scope of this work.
The results presented in the previous sections have several applications. They introduce a broader perspective for assessing the predictability of ice conditions for forecasting and operational activities and also a diagnostic to evaluate climate model capabilities to simulate the adequate conditions for ecosystem studies (e.g. Williams et al., 2014; Rogers et al., 2020; Meynecke et al., 2021). Due to its construction, the method should be mostly applied in climatological or medium- to long-term investigations of ice variability. Here the full record has been used to define the climatology, but climatological baselines for different periods can be computed to detect changes in the variability with time. It may also be used in an operational context, for instance comparing each daily anomaly against the long-term distribution of anomalies in a particular region. This has not however been verified in this analysis and would deserve dedicated work. From an operational viewpoint, the exceedance maps can be used to plan scientific and logistical activities in seasonally ice-covered Southern Ocean waters. This method should not be used to measure the extent of pack ice conditions because multi-year ice is not counted due to its high persistence and reduced inter-annual variability. Finally, the possibility of seeing patterns of intensity within the region classified as MIZ would allow the identification of further linkages with the atmospheric boundary layer, for instance looking for associations between regions of high synoptic variability and corresponding changes in the character of Antarctic sea ice.
The EUMETSAT OSI-450 CDR product is available at http://doi.org/10.15770/EUM_SAF_OSI_0008 (OSI SAF, 2017), and the NOAA/NSIDC Climate Data Record of Passive Microwave Sea Ice Concentration, Version 4, can be downloaded from https://doi.org/10.7265/efmz-2t65 (Meier et al., 2021). The code used to process the data and produce the figures is available at https://doi.org/10.25375/uct.21103363.v1 (Vichi, 2022a), and the climatological data in NetCDF format are available at https://doi.org/10.5281/zenodo.7077675 (Vichi, 2022b).
The supplement related to this article is available online at: https://doi.org/10.5194/tc-16-4087-2022-supplement.
The author has declared that there are no competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
This work has emerged from a collaboration of multiple projects: the South African National Antarctic Programme, the Earth System Science Research Program, and the Whales and Climate research program (https://whalesandclimate.org, last access: 5 October 2022). I would like to thank the NOAA/NSIDC support team for the prompt assistance and help in reprocessing the CDR V4 dataset. I am also grateful to the anonymous reviewers, who gave critical insights based on an earlier version of this manuscript.
This research has been supported by the National Research Foundation of South Africa (grant nos. 118745 and 118598). This work has received funding from the European Union’s Horizon 2020 research and innovation programme under grant agreement no. 101003826 via project CRiceS (Climate Relevant interactions and feedbacks: the key role of sea ice and Snow in the polar and global climate system).
This paper was edited by Ludovic Brucker and reviewed by two anonymous referees.
Alberello, A., Onorato, M., Bennetts, L., Vichi, M., Eayrs, C., MacHutchon, K., and Toffoli, A.: Brief communication: Pancake ice floe size distribution during the winter expansion of the Antarctic marginal ice zone, The Cryosphere, 13, 41–48, https://doi.org/10.5194/tc-13-41-2019, 2019. a
Alberello, A., Bennetts, L., Heil, P., Eayrs, C., Vichi, M., MacHutchon, K., Onorato, M., and Toffoli, A.: Drift of Pancake Ice Floes in the Winter Antarctic Marginal Ice Zone During Polar Cyclones, J. Geophys. Res.-Oceans, 125, e2019JC015418, https://doi.org/10.1029/2019JC015418, 2020. a
Andreas, E. L., Lange, M. A., Ackley, S. F., and Wadhams, P.: Roughness of Weddell Sea Ice and Estimates of the Air–Ice Drag Coefficient, J. Geophys. Res.-Oceans, 98, 12439–12452, 1993. a
Bigdeli, A., Hara, T., Loose, B., and Nguyen, A. T.: Wave Attenuation and Gas Exchange Velocity in Marginal Sea Ice Zone, J. Geophys. Res.-Oceans, 123, 2293–2304, https://doi.org/10.1002/2017JC013380, 2018. a
Castellani, G., Losch, M., Ungermann, M., and Gerdes, R.: Sea-Ice Drag as a Function of Deformation and Ice Cover: Effects on Simulated Sea Ice and Ocean Circulation in the Arctic, Ocean Model., 128, 48–66, https://doi.org/10.1016/j.ocemod.2018.06.002, 2018. a
Comiso, J. C. and Zwally, H. J.: Concentration Gradients and Growth/Decay Characteristics of the Seasonal Sea Ice Cover, J. Geophys. Res.-Oceans, 89, 8081–8103, https://doi.org/10.1029/JC089iC05p08081, 1984. a, b
de Jager, W. and Vichi, M.: Rotational drift in Antarctic sea ice: pronounced cyclonic features and differences between data products, The Cryosphere, 16, 925–940, https://doi.org/10.5194/tc-16-925-2022, 2022. a
Dumont, D., Kohout, A., and Bertino, L.: A Wave-Based Model for the Marginal Ice Zone Including a Floe Breaking Parameterization, J. Geophys. Res.-Oceans, 116, C04001, https://doi.org/10.1029/2010JC006682, 2011. a
Eayrs, C., Holland, D., Francis, D., Wagner, T., Kumar, R., and Li, X.: Understanding the Seasonal Cycle of Antarctic Sea Ice Extent in the Context of Longer-Term Variability, Rev. Geophys., 57, 1037–1064, https://doi.org/10.1029/2018RG000631, 2019. a
Gupta, M., Follows, M. J., and Lauderdale, J. M.: The Effect of Antarctic Sea Ice on Southern Ocean Carbon Outgassing: Capping Versus Light Attenuation, Global Biogeochem. Cy., 34, e2019GB006489, https://doi.org/10.1029/2019GB006489, 2020. a
Haumann, F. A., Moorman, R., Riser, S. C., Smedsrud, L. H., Maksym, T., Wong, A. P. S., Wilson, E. A., Drucker, R., Talley, L. D., Johnson, K. S., Key, R. M., and Sarmiento, J. L.: Supercooled Southern Ocean Waters, Geophys. Res. Lett., 47, e2020GL090242, https://doi.org/10.1029/2020GL090242, 2020. a
Hepworth, E., Messori, G., and Vichi, M.: Association Between Extreme Atmospheric Anomalies Over Antarctic Sea Ice, Southern Ocean Polar Cyclones and Atmospheric Rivers, J. Geophys. Res.-Atmos., 127, e2021JD036121, https://doi.org/10.1029/2021JD036121, 2022. a
Hogg, J., Fonoberova, M., and Mezić, I.: Exponentially Decaying Modes and Long-Term Prediction of Sea Ice Concentration Using Koopman Mode Decomposition, Sci. Rep.-UK, 10, 16313, https://doi.org/10.1038/s41598-020-73211-z, 2020. a
Kern, S., Lavergne, T., Notz, D., Pedersen, L. T., Tonboe, R. T., Saldo, R., and Sørensen, A. M.: Satellite passive microwave sea-ice concentration data set intercomparison: closed ice and ship-based observations, The Cryosphere, 13, 3261–3307, https://doi.org/10.5194/tc-13-3261-2019, 2019. a, b
Kohout, A. L., Williams, M. J. M., Dean, S. M., and Meylan, M. H.: Storm-Induced Sea-Ice Breakup and the Implications for Ice Extent, Nature, 509, 604–607, https://doi.org/10.1038/nature13262, 2014. a, b
Kohout, A. L., Smith, M., Roach, L. A., Williams, G., Montiel, F., and Williams, M. J. M.: Observations of Exponential Wave Attenuation in Antarctic Sea Ice during the PIPERS Campaign, Ann. Glaciol., 61, 196–209, https://doi.org/10.1017/aog.2020.36, 2020. a, b
Lavergne, T., Sørensen, A. M., Kern, S., Tonboe, R., Notz, D., Aaboe, S., Bell, L., Dybkjær, G., Eastwood, S., Gabarro, C., Heygster, G., Killie, M. A., Brandt Kreiner, M., Lavelle, J., Saldo, R., Sandven, S., and Pedersen, L. T.: Version 2 of the EUMETSAT OSI SAF and ESA CCI sea-ice concentration climate data records, The Cryosphere, 13, 49–78, https://doi.org/10.5194/tc-13-49-2019, 2019. a, b
Lavergne, T., Kern, S., Aaboe, S., Derby, L., Dybkjaer, G., Garric, G., Heil, P., Hendricks, S., Holfort, J., Howell, S., Key, J., Lieser, J. L., Maksym, T., Maslowski, W., Meier, W., Muñoz-Sabater, J., Nicolas, J., Özsoy, B., Rabe, B., Rack, W., Raphael, M., de Rosnay, P., Smolyanitsky, V., Tietsche, S., Ukita, J., Vichi, M., Wagner, P., Willmes, S., and Zhao, X.: A New Structure for the Sea Ice Essential Climate Variables of the Global Climate Observing System, B. Am. Meteorol. Soc., 103, E1502–E1521, https://doi.org/10.1175/BAMS-D-21-0227.1, 2022. a
Maksym, T.: Arctic and Antarctic Sea Ice Change: Contrasts, Commonalities, and Causes, Annu. Rev. Mar. Sci., 11, 187–213, https://doi.org/10.1146/annurev-marine-010816-060610, 2019. a
Martinson, D. G. and Iannuzzi, R. A.: Antarctic Ocean-Ice Interaction: Implications from Ocean Bulk Property Distributions in the Weddell Gyre, in: Antarctic Sea Ice: Physical Processes, Interactions and Variability, edited by: Jeffries, M. O., American Geophysical Union (AGU), https://doi.org/10.1029/AR074p0243, pp. 243–271, 1998. a
Massom, R. A., Scambos, T. A., Bennetts, L. G., Reid, P., Squire, V. A., and Stammerjohn, S. E.: Antarctic Ice Shelf Disintegration Triggered by Sea Ice Loss and Ocean Swell, Nature, 558, 383, https://doi.org/10.1038/s41586-018-0212-1, 2018. a, b
Matear, R. J., O'Kane, T. J., Risbey, J. S., and Chamberlain, M.: Sources of Heterogeneous Variability and Trends in Antarctic Sea-Ice, Nat. Commun., 6, 8656, https://doi.org/10.1038/ncomms9656, 2015. a, b
Meier, W. N. and Stroeve, J.: Comparison of Sea-Ice Extent and Ice-Edge Location Estimates from Passive Microwave and Enhanced-Resolution Scatterometer Data, Ann. Glaciol., 48, 65–70, https://doi.org/10.3189/172756408784700743, 2008. a
Meier, W. N., Peng, G., Scott, D. J., and Savoie, M. H.: Verification of a New NOAA/NSIDC Passive Microwave Sea-Ice Concentration Climate Record, Polar Res., 33, https://doi.org/10.3402/polar.v33.21004, 2014. a
Meier, W. N., Fetterer, F., Savoie, M. H., Mallory, M., Duerr, R., and Stroeve, J. C.: NOAA/NSIDC Climate Data Record of Passive Microwave Sea Ice Concentration, Version 3, National Snow and Ice Data Center [data set], https://doi.org/10.7265/N59P2ZTG, 2017. a
Meier, W. N., Fetterer, F., Windnagel, A. K., and Stewart, J. S.: NOAA/NSIDC Climate Data Record of Passive Microwave Sea Ice Concentration, Version 4, Boulder, Colorado USA, National Snow and Ice Data Center [data set], https://doi.org/10.7265/efmz-2t65, 2021. a, b
Meynecke, J.-O., de Bie, J., Barraqueta, J.-L. M., Seyboth, E., Dey, S. P., Lee, S. B., Samanta, S., Vichi, M., Findlay, K., Roychoudhury, A., and Mackey, B.: The Role of Environmental Drivers in Humpback Whale Distribution, Movement and Behavior: A Review, Frontiers in Marine Science, 8, 1685, https://doi.org/10.3389/fmars.2021.720774, 2021. a
Mosig, J. E., Montiel, F., and Squire, V. A.: Comparison of Viscoelastic-Type Models for Ocean Wave Attenuation in Ice-Covered Seas, J. Geophys. Res.-Oceans, 120, 6072–6090, https://doi.org/10.1002/2015JC010881, 2015. a
Parkinson, C. L.: A 40-y Record Reveals Gradual Antarctic Sea Ice Increases Followed by Decreases at Rates Far Exceeding the Rates Seen in the Arctic, P. Natl. Acad. Sci. USA, 116, 14414–14423, https://doi.org/10.1073/pnas.1906556116, 2019. a, b, c
Paul, F., Mielke, T., Schwarz, C., Schröder, J., Rampai, T., Skatulla, S., Audh, R. R., Hepworth, E., Vichi, M., and Lupascu, D. C.: Frazil Ice in the Antarctic Marginal Ice Zone, Journal of Marine Science and Engineering, 9, 647, https://doi.org/10.3390/jmse9060647, 2021. a
Peng, G., Meier, W. N., Scott, D. J., and Savoie, M. H.: A long-term and reproducible passive microwave sea ice concentration data record for climate studies and monitoring, Earth Syst. Sci. Data, 5, 311–318, https://doi.org/10.5194/essd-5-311-2013, 2013. a
Petrich, C. and Eicken, H.: Overview of Sea Ice Growth and Properties, chap. 1, in: Sea Ice, edited by: Thomas, D. N., John Wiley & Sons, Ltd, https://doi.org/10.1002/9781118778371.ch1, pp. 1–41, 2017. a
Raphael, M. N. and Hobbs, W.: The Influence of the Large-Scale Atmospheric Circulation on Antarctic Sea Ice during Ice Advance and Retreat Seasons, Geophys. Res. Lett., 41, 5037–5045, https://doi.org/10.1002/2014GL060365, 2014. a
Rogers, A., Frinault, B., Barnes, D., Bindoff, N., Downie, R., Ducklow, H., Friedlaender, A., Hart, T., Hill, S., Hofmann, E., Linse, K., McMahon, C., Murphy, E., Pakhomov, E., Reygondeau, G., Staniland, I., Wolf-Gladrow, D., and Wright, R.: Antarctic Futures: An Assessment of Climate-Driven Changes in Ecosystem Structure, Function, and Service Provisioning in the Southern Ocean, Annu. Rev. Mar. Sci., 12, 87–120, https://doi.org/10.1146/annurev-marine-010419-011028, 2020. a
Squire, V. A.: Ocean Wave Interactions with Sea Ice: A Reappraisal, Annu. Rev. Fluid Mech., 52, 37–60, https://doi.org/10.1146/annurev-fluid-010719-060301, 2020. a, b, c
Steele, M., Morison, J. H., and Untersteiner, N.: The Partition of Air–Ice–Ocean Momentum Exchange as a Function of Ice Concentration, Floe Size, and Draft, J. Geophys. Res.-Oceans, 94, 12739–12750, https://doi.org/10.1029/JC094iC09p12739, 1989. a
Stopa, J. E., Ardhuin, F., Thomson, J., Smith, M. M., Kohout, A., Doble, M., and Wadhams, P.: Wave Attenuation Through an Arctic Marginal Ice Zone on 12 October 2015: 1. Measurement of Wave Spectra and Ice Features From Sentinel 1A, J. Geophys. Res.-Oceans, 123, 3619–3634, https://doi.org/10.1029/2018JC013791, 2018. a, b
Stroeve, J. C., Jenouvrier, S., Campbell, G. G., Barbraud, C., and Delord, K.: Mapping and assessing variability in the Antarctic marginal ice zone, pack ice and coastal polynyas in two sea ice algorithms with implications on breeding success of snow petrels, The Cryosphere, 10, 1823–1843, https://doi.org/10.5194/tc-10-1823-2016, 2016. a, b, c, d, e, f, g, h, i
Strong, C.: Atmospheric Influence on Arctic Marginal Ice Zone Position and Width in the Atlantic Sector, February–April 1979–2010, Clim. Dyn., 39, 3091–3102, https://doi.org/10.1007/s00382-012-1356-6, 2012. a
Strong, C., Foster, D., Cherkaev, E., Eisenman, I., and Golden, K. M.: On the Definition of Marginal Ice Zone Width, J. Atmos. Ocean. Tech., 34, 1565–1584, https://doi.org/10.1175/JTECH-D-16-0171.1, 2017. a, b
Turner, J., Phillips, T., Marshall, G. J., Hosking, J. S., Pope, J. O., Bracegirdle, T. J., and Deb, P.: Unprecedented Springtime Retreat of Antarctic Sea Ice in 2016, Geophys. Res. Lett., 44, 6868–6875, https://doi.org/10.1002/2017GL073656, 2017. a, b
Vichi, M., Eayrs, C., Alberello, A., Bekker, A., Bennetts, L., Holland, D., de Jong, E., Joubert, W., MacHutchon, K., Messori, G., Mojica, J. F., Onorato, M., Saunders, C., Skatulla, S., and Toffoli, A.: Effects of an Explosive Polar Cyclone Crossing the Antarctic Marginal Ice Zone, Geophys. Res. Lett., 46, 5948–5958, https://doi.org/10.1029/2019GL082457, 2019. a, b, c, d, e, f, g
Weeks, W. F.: On Sea Ice, University of Alaska Press, Fairbanks, ISBN 978-1-60223-079-8, 2010. a
Weeks, W. F. and Ackley, S. F.: The Growth, Structure, and Properties of Sea Ice, in: The Geophysics of Sea Ice, edited by: Untersteiner, N., NATO ASI Series, Springer US, Boston, MA, https://doi.org/10.1007/978-1-4899-5352-0_2, pp. 9–164, 1986. a
Williams, R., Kelly, N., Boebel, O., Friedlaender, A. S., Herr, H., Kock, K.-H., Lehnert, L. S., Maksym, T., Roberts, J., Scheidat, M., Siebert, U., and Brierley, A. S.: Counting Whales in a Challenging, Changing Environment, Sci. Rep.-UK, 4, 4170, https://doi.org/10.1038/srep04170, 2014. a
Williams, T. D., Bennetts, L. G., Squire, V. A., Dumont, D., and Bertino, L.: Wave–Ice Interactions in the Marginal Ice Zone. Part 2: Numerical Implementation and Sensitivity Studies along 1D Transects of the Ocean Surface, Ocean Model., 71, 92–101, https://doi.org/10.1016/j.ocemod.2013.05.011, 2013. a, b
Windnagel, A., Meier, W., Stewart, S., Fetterer, F., and Stafford, T.: NOAA/NSIDC Climate Data Record of Passive Microwave Sea Ice Concentration, Version 4 Analysis, Special Report #20, National Snow and Ice Data Center [data set], https://doi.org/10.7265/EFMZ-2T65, 2021. a, b
WMO: WMO Sea-Ice Nomenclature, no. 259 in WMO, World Meteorological Organization, Geneva, https://library.wmo.int/doc_num.php?explnum_id=4651 (last access: 5 October 2022), 2014. a
WMO: Sea-Ice Information and Services, no. 574 in WMO, World Meteorological Organization, Geneva, 2021 edition, https://library.wmo.int/doc_num.php?explnum_id=10763 (last access: 5 October 2022), 2021. a
Womack, A., Vichi, M., Alberello, A., and Toffoli, A.: Atmospheric Drivers of a Winter-to-Spring Lagrangian Sea-Ice Drift in the Eastern Antarctic Marginal Ice Zone, J. Glaciol., 68, 999–1013, https://doi.org/10.1017/jog.2022.14, 2022. a, b, c, d, e
Worby, A. P., Jeffries, M. O., Weeks, W. F., Morris, K., and Jaña, R.: The Thickness Distribution of Sea Ice and Snow Cover during Late Winter in the Bellingshausen and Amundsen Seas, Antarctica, J. Geophys. Res.-Oceans, 101, 28441–28455, https://doi.org/10.1029/96JC02737, 1996. a
Yuan, N., Ding, M., Ludescher, J., and Bunde, A.: Increase of the Antarctic Sea Ice Extent Is Highly Significant Only in the Ross Sea, Sci. Rep.-UK, 7, 41096, https://doi.org/10.1038/srep41096, 2017. a