Journal topic
The Cryosphere, 12, 2595–2607, 2018
https://doi.org/10.5194/tc-12-2595-2018
The Cryosphere, 12, 2595–2607, 2018
https://doi.org/10.5194/tc-12-2595-2018

Research article 14 Aug 2018

Research article | 14 Aug 2018

# Estimation of Arctic land-fast ice cover based on dual-polarized Sentinel-1 SAR imagery

Estimation of Arctic land-fast ice cover based on dual-polarized Sentinel-1 SAR imagery
Juha Karvonen Juha Karvonen
• Finnish Meteorological Institute, PB 503, 00101, Helsinki, Finland

Correspondence: Juha Karvonen (juha.karvonen@fmi.fi)

Abstract

Here a method for estimating the land-fast ice (LFI) extent from dual-polarized Sentinel-1 SAR mosaics of an Arctic study area over the Kara and Barents seas is presented. The method is based on temporal cross-correlation between adjacent daily SAR mosaics. The results are compared to the LFI of the Russian Arctic and Antarctic Research Institute (AARI) ice charts. Two versions of the method were studied: in the first version (FMI-A) the overall performance was optimized, and in the second version (FMI-B) the target was a low LFI misdetection rate. FMI-A detected over 73 % of the AARI ice chart LFI, and FMI-B a little over 50 % of the AARI ice chart LFI. During the winter months the detection rates were higher than during the melt-down season for both the studied algorithm versions. An LFI time series covering the time period from October 2015 to the end of August 2017 computed using the proposed methodology is provided on the FMI ftp server. The time series will be extended twice annually.

1 Introduction

Land-fast ice (also known as shore-fast ice, or fast ice for short), here denoted by LFI, is sea ice attached to the coastline, to the sea floor along shallow areas or to grounded icebergs . LFI may either grow in place from the seawater or by freezing drifting ice to the shore (JCOMM 2015). LFI does not move with currents and winds. LFI zone is typically seasonal and depends on ice thickness, topography of the sea floor and islands . On average the fast ice edge is located at the water depth of 10–25 m . However, there exists seasonal and inter-annual variability. Based on the numbers given (e.g., ) LFI area covers approximately 13 % of the Northern Hemisphere area of sea ice cover and thus represents an essential fraction of the Arctic sea ice. LFI zone distance from the coast varies from a few meters to several hundreds of kilometers (JCOMM 2015). For practical LFI detection some criteria to detect the LFI areas need to be fixed. In two criteria have been used for LFI: the ice is contiguous with land and it lacks detectable motion for approximately 20 days. In the methodology presented here a two-week period without ice motion and contiguousness with land have been used as criteria for LFI.

Long-term changes have been found in the LFI regime. The trend seems to be toward reducing LFI area , later formation and earlier disappearance , and reduction of the LFI thickness . Although LFI zone only covers a relatively small fraction of the total Arctic sea ice extent, it has particular importance for the coastal systems, for example, by defining the location of polynyas . These facts make monitoring of the Arctic LFI zone important, also as a climate change indicator.

LFI detection based on different techniques and different instruments have been proposed previously. Passive microwave (PM) data have been widely used for determining sea ice motion (e.g., , and ), but because of their low spatial resolution (5–50 km) PM data have not been used much for fast ice detection . Some examples of using PM data for LFI estimation exist. For example, temporal correlation median of AMSR-E imagery was used for LFI detection in . High-resolution near-infrared imagery from Landsat I and II has been used for identification of Alaska LFI as sea ice contiguous with the coast . A method for estimating LFI using cloudless spectroradiometer (MODIS) data was proposed in . The method uses a 20-day composite of MODIS imagery of eastern Antarctic coast additionally supported by the AMSR-E ASI algorithm sea ice concentration in the case of unreliable (possibly cloudy) MODIS image composites. In machine learning (random forest algorithm) using data from multiple instruments – AMSR-E brightness temperature, MODIS ice surface temperature (IST), and SSMI (Special Sensor Microwave/Imager) ice velocity – was applied to detect LFI. In the study ice velocity and IST proved to be the most significant factors in LFI detection.

Also different methods utilizing SAR imagery for LFI detection have been proposed. Significant advantages of using SAR imagery are the high resolution, typically from tens to a few hundreds of meters, of SAR imagery and the capability to measure in cloudy or dark (no daylight) conditions. Sentinel-1 temporal cover in the Arctic is comparable to that of a radiometer (e.g., AMSR-2) data. In the areas of static ice were determined manually from consecutive SAR images (time series). In LFI was detected based on vector grayscale gradient fields of three subsequent SAR images. The bottom fast ice zone can be identified based on the SAR backscatter magnitude because if there is no ice–water interface the dielectric contrast at the bottom is significantly reduced. Ice drift can also be derived from multi-temporal SAR image pairs over the same area. Such SAR ice drift detection algorithms are typically based on temporal cross-correlation; that is, cross-correlation between co-registered spatially (partly) overlapping SAR images acquired at different time instants , temporal phase correlation or optical flow (Sun1996). From time series of ice drift estimates it is possible to derive the static ice areas which can then be interpreted as LFI, assuming the time series of ice drift at a certain location is long enough. Also SAR interferometry can be used for LFI detection , as the phase difference is random for drift ice and coherent for the static ice fields. However, the availability of Single Look Complex (SLC) SAR data required for SAR interferometry is currently restricted, and thus methods based on SAR interferometry are not yet suitable for LFI monitoring in a large spatial scale. In the cumulative Baltic sea ice drift estimated from multi-temporal SAR imagery was used for locating the Baltic sea LFI by indicating the areas where no ice motion had occurred within a predefined and long-enough time period (typically around two weeks). In temporal cross-correlation minimum was used to locate LFI to aid sea ice concentration estimation.

Figure 1The study area in the used polar stereographic projection.

The algorithms proposed in this study are used for creating daily time series of the Kara and Barents sea LFI extent in a high resolution (500 m) gradually complementing the existing Arctic LFI time series derivable from Arctic operational ice charts. FMI has some sea ice products which have been run in an operational test mode during a few winters over the studied area. The aim is to include the LFI estimation in the FMI operational Arctic sea ice product portfolio. Technical details of the FMI operational Arctic sea ice thickness and concentration test products can be found in and . One purpose is to utilize the LFI algorithm result first to locate the static ice fields and then apply the FMI HIGH-resolution Thermodynamic Snow/Ice model (HIGHTSI) to estimate the ice growth or melt during the static ice periods to improve the ice thickness estimates over the static ice areas. In the static parts of the LFI zone (during the long static periods) only thermodynamic ice modeling can be applied as the dynamic part can be omitted for the static ice. This will increase the reliability of ice modeling in the static ice areas, assuming that the static ice areas can reliably be located, as the ice thickness uncertainties originating from the ice dynamics will then be excluded.

Figure 2SAR mosaics of 8 March 2016: HH mosaic (a) and HV mosaic (b). The land areas appear as green and areas of no data as black.

2 Study area, data sets and pre-processing

## 2.1 Study area

The study area is located in the Kara and Barents seas. The study area is shown in Fig. 1. The coordinate system (CS) used in this paper is the polar stereographic projection, with a center longitude of 55 E, reference latitude (latitude of the correct scale) of 70 N and the WGS84 datum. The upper left (UL) and lower right (LR) coordinates in this CS are the following (polar stereographic CS northing and easting in meters): UL $=\left(-\mathrm{700}\phantom{\rule{0.125em}{0ex}}\mathrm{000},-\mathrm{1}\phantom{\rule{0.125em}{0ex}}\mathrm{100}\phantom{\rule{0.125em}{0ex}}\mathrm{000}\right)$ and LR $=\left(-\mathrm{2}\phantom{\rule{0.125em}{0ex}}\mathrm{550}\phantom{\rule{0.125em}{0ex}}\mathrm{000},\mathrm{1}\phantom{\rule{0.125em}{0ex}}\mathrm{100}\phantom{\rule{0.125em}{0ex}}\mathrm{000}\right)$.

## 2.2 Russian ice charts

The Russian Arctic ice charts are provided weekly by the Arctic and Antarctic Research Institute (AARI) on their web page (the English version on http://www.aari.ru/odata/_d0015.php?lang=1, last access: 1 March 2018). They are provided as thematic maps and in SIGRID-3 vector format (JCOMM2014) in the polar stereographic projection with the mid-longitude of 90 E. In this study the AARI ice chart thematic maps were reprojected into the polar stereographic projection used in this study, and the LFI areas were extracted based on the colormap of the AARI ice charts. In this study 51 AARI ice charts of the period from November 2015 to October 2016, covering a whole year time, were used as reference LFI data for defining the algorithm parameters and to evaluate the proposed algorithms. Actually, four AARI ice charts (one ice chart of each month in the period January–April 2016) were used for defining the optimal algorithm threshold parameters, and the remaining 47 ice charts were used for evaluation. The study area was cropped from the weekly reprojected AARI ice charts, and the cropped images were converted into binary 1 bit per pixel images in which the LFI areas, appearing as white in the AARI ice chart maps (for an example of an AARI ice chart see Fig. 6), were mapped to the pixel value of one and the rest of the image was mapped to the pixel value of zero.

Figure 3Block diagram of the LFI detection (FMI-A) for Sentinel-1 HH polarization channel. The process for the HV channel is similar, except that a threshold value of THV is applied instead of THH.

## 2.3 Sentinel-1 imagery, SAR mosaic and their processing

All the available European Space Agency's (ESA) C-band Sentinel-1 dual-polarized extra-wide (EW) swath mode level 1 ground range detected medium-resolution (GRDM) data with the HH/HV polarization channels over the study area during the study period (October 2015–August 2017) were used in this study. The Sentinel-1 SAR data are publicly available through the Copernicus Science Hub (https://scihub.copernicus.eu/, last access: 8 August 2018). The imagery was preprocessed by applying an incidence angle correction to the HH channel and a combined incidence angle and noise floor correction to the HV channel. For details on this process, see . After incidence angle and noise floor corrections the image data were geo-rectified into the polar stereographic projection specified in Sect. 2.1. After geo-rectification the imagery was still down-sampled to 500 m resolution, and finally the daily mosaics were constructed by overlaying the newer images over the older ones such that for each mosaic grid cell (pixel) the newest SAR data prior to the mosaic time label, which was defined to be 12:00 UTC daily here, were assigned to it. The mosaics were cumulative, meaning that the newer imagery was always overlaid over the previous mosaic, and the mosaic was initialized only in the beginning of the mosaicking (in this case in the beginning October 2015). In practice the data at a given grid cell location were no older than 3 days compared to the mosaic time label, as Sentinel-1 temporal cover over the European Arctic is so good. Separate mosaics for HH and HV channels were constructed. A land mask based on the Global Self-consistent, Hierarchical, High-resolution Geography database (GSHHG) coastline data set was applied to the mosaics to exclude land areas from LFI computation. As an example of SAR mosaics the mosaics for HH and HV channels of 8 March 2016 with the land masking are shown in Fig. 2. Dual-polarized EW mode Sentinel-1 data are systematically acquired over the European Arctic and Greenland waters by ESA, but over the other Arctic areas a single-polarization (HH) mode is used. Near the upper right corner of the study area there were no dual-polarized Sentinel-1 EW mode data available, because this area belongs to the single-polarization HH mode acquisition area defined by ESA. This can also be seen as the black area in Fig. 2.

3 Methodology for estimation of land-fast ice areas

The proposed LFI estimation process for a single SAR channel is presented in Fig. 3. Similar processing is performed for both the SAR channels (HH and HV), and the results are combined after computing the channel-wise LFI estimates. In the first phase the SAR mosaics are generated as described in Sect. 2. These mosaics (red boxes in Fig. 3) of a two-week period are the inputs to the cross-correlation computation phase (indicated by yellow color in Fig. 3).

To increase the computation performance and to exclude areas where LFI does not appear, a mask indicating the potential LFI zone as the areas of 100 km or less from the coastline (including islands) was produced. The mask was produced iteratively starting from the coastline, indicated by the land mask. The distance to the (nearest) coast was iteratively increased by 500 m (pixel size) for the vertical and horizontal neighbor pixels and by $\sqrt{\mathrm{2}}×\mathrm{500}$ m for the diagonal neighbor pixels of the pixels with a distance from the coast already assigned to them. This was iterated until there were no more distances less than 100 km (corresponding to 200 grid pixels) from the coast within the study area grid. The use of the proposed mask did not have any effect on the LFI detection, and it was used here just to fasten the processing. The execution time for a single-day LFI estimation was not very long (several minutes), but for longer LFI time series the difference of execution times with the mask and without the mask was significant, and therefore the mask has systematically been applied in this study. The masking here applied this simple approach; however, in some other areas a more sophisticated mask taking into account the bathymetry, for example, using a given distance from the depth of 25 m, might be more useful. The mask applied is shown in Fig. 4. Unfortunately FMI did not have very accurate bathymetry data over the study area available, and thus only this simple mask was applied here. With a more accurate mask possibly more time could be saved in computation of LFI time series. This masking step is indicated by green color in Fig. 3.

Figure 4Mask used to locate the areas where LFI is searched. White areas indicate the LFI search area and green areas are land.

Figure 5The total number of erroneously classified pixels as a function of the temporal cross-correlation average for HH channel SAR data (a) and for HV channel SAR data (b). The optimal thresholds were defined as the minimum of the total error (“sum” curves according to the legends).

The temporal cross-correlation, denoted by CT, between SAR mosaics of two adjacent days was computed as

$\begin{array}{ll}& {C}_{\mathrm{T}}\left(r,c,t\right)=\frac{\mathrm{1}}{\mathit{\sigma }\left(r,c,t\right)\mathit{\sigma }\left(r,c,t-\mathrm{1}\right)}\sum _{i,j\in W}\\ & \phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\left(M\left(r+i,c+j,t\right)-\mathit{\mu }\left(r,c,t\right)\right)\\ \text{(1)}& & \phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\left(M\left(r+i,c+j,t-\mathrm{1}\right)-\mathit{\mu }\left(r,c,t-\mathrm{1}\right)\right).\end{array}$

The indices r and c refer to the pixel location (row and column coordinates), t refers to the day (t−1 refers to the previous day of the day t), and CT is computed within a round-shaped window W with a radius R around the pixel at the location (r, c). In this study the value R=3 was used. $M\left(r,c,t\right)$ refers to a mosaic pixel value at the location (r, c) on day t. The means $\mathit{\mu }\left(r,c,t\right)$ and standard deviations $\mathit{\sigma }\left(r,c,t\right)$ are computed over W. The mosaics of the two adjacent days in the computation of CT were also always mosaics of the same polarization, either HH or HV. The cross-correlation computation is indicated by yellow color in Fig. 3. To reduce computation, pixel-wise CT between two adjacent days' mosaics was also computed only over the areas defined by the distance (from the coast) mask (i.e., white areas in Fig. 4).

After computing the CT grids the temporal 14-day average (blue box in Fig. 3) of the daily CT grids are computed. The areas where CT is close to 1 (higher than 0.95) are excluded from the average computation, as they represent areas where the mosaic has not updated since the previous day. For SAR data from two different SAR images CT is in practice always less than 1, and even less than 0.95, which is used as a threshold here, because the speckle present in all radar imagery CT is decreased even for a static target present at the same location in both of the mosaics of a mosaic pair. The initial decision of whether a pixel represents LFI or does not is made based on thresholding of the TC average (red color in Fig. 3). The thresholds for the HH and HV SAR channels were studied by varying the threshold value and then comparing the LFI area detected by thresholding and LFI area of four AARI ice charts of the period January–April 2016: one ice chart for each month was used for defining the thresholds. The optimal thresholds were defined by minimizing the estimation error (i.e., the sum of LFI not detected by the algorithm and non-LFI classified as LFI by the algorithm when compared to the AARI ice chart LFI). The optimal thresholds yielded were THH=0.31 and THV=0.24 for HH and HV channel mosaics, respectively. The classification error as a function of CT for both the channels can be seen in Fig. 5. These curves can be used for deriving the thresholds THH and THV. Here we have applied a criterion minimizing the total classification error, but also other criteria, depending on the objective, could be considered. At this stage a grid cell is considered as a possible LFI pixel if the conditions for the channel-wise cross-correlation averages (${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HH}}$ and ${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HV}}$) ${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HH}}>{T}_{\mathrm{HH}}$ and ${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HV}}>{T}_{\mathrm{HV}}$ apply and they are in the area defined by the distance mask (white areas of Fig. 4).

After applying the thresholding to ${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HH}}$ and ${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HV}}$ a morphological opening operation (i.e., an erosion operation followed by a dilation operation) by a disk with a radius of two pixels is applied to remove narrow elongated, high ${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}$ segments and small single patches. This operation is indicated by the gray color in Fig. 3. Narrow elongated segments may appear due to the boundaries of SAR frames over open water, where the incidence angle correction often fails because of varying wave conditions in different SAR frames in a mosaic. Small single patches may be caused by random noise or be due to possible small static targets. After applying the morphological opening operator, removal of small LFI segments is applied. This filtering stage is indicated by the white box in Fig. 3. The small segment filtering performs removal of segment smaller than a given threshold value (Ts). Here the value Ts=100 pixels, corresponding to an area of 25 km2, has been applied. This post-filtering also efficiently reduces the number small erroneous segments due to SAR artifacts and speckle. The same procedure is performed for the HH and HV SAR channels with the only difference of applying a different threshold value (THH or THV) depending on the SAR channel in thresholding of the temporal cross-correlation average (${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HH}}$ or ${\stackrel{\mathrm{‾}}{C}}_{\mathrm{T}}^{\mathrm{HV}}$).

After retrieving the channel-wise LFI area estimates for the HH and HV channels, the LFI estimation results of the two SAR channels (LFIHH and LFIHV) are combined by applying a logical AND operator between the channel-wise binary classification results. Finally, areas which are not connected (in the sense of 8-pixel neighborhood) to land area defined by the land mask are excluded from the LFI class. This is in practice performed by applying a recursive flood-fill algorithm testing the filled pixel neighbors for land (land mask pixels) while filling each contiguous LFI candidate segment produced by the earlier preliminary classification. This result is referred to here as method A, FMI-A for short.

To further reduce the erroneous non-LFI classification to the LFI category by FMI-A, an additional temporal logical AND operation applied to 14 adjacent-day FMI-A products was performed. Application of the logical AND gives the areas where there was LFI in each daily FMI-A classification during the two-week period. The result after the logical AND operation is referred to here as method B (FMI-B).

4 Results

The results were first computed for a test data set over a one-year period from November 2015 to November 2016, and the results were compared with the weekly AARI ice charts. The comparison was pixel-based and it was performed between the daily LFI products and the corresponding AARI LFI of the same date (ice chart issuing date). The daily LFI products were the LFI estimates produced by FMI-A and FMI-B using the SAR mosaic of the LFI product issuing date and SAR mosaics of the preceding two-week time period. In total, 47 weekly AARI ice charts were used in the comparison (the exact period was from 3 November 2015 to 1 November 2016). Four weekly AARI ice charts used in defining the algorithm thresholds were excluded from the numerical comparisons. Because FMI-A also suggested a little amount of LFI during the summer, and these summer LFI areas were the same areas for both the summers included in the study, the summer LFI areas suggested by FMI-A in August 2016 were filtered out (subtracted) from all the FMI-A and FMI-B products. It was assumed that these summer LFI detections were due to inaccuracies in the land mask.

Table 1Comparison of the FMI methods to AARI ice charts; the numbers are in percents. The values in parentheses are standard deviations in percentage points of the AARI ice chart LFI.

Figure 6AARI ice chart of 8 March 2016, translated into the polar stereographic projection used in this study and cropped to the study area.

Figure 7LFI extent based on AARI ice chart (a), FMI-A LFI (b) and FMI-B LFI (c) of 8 March 2016. LFI areas are the black areas.

Figure 8Monthly detection and false detection percentages for FMI-A (a) and FMI-B (b) compared to AARI ice chart LFI, and the relative number of (AARI) LFI points (c) in percents of the AARI LFI points of the whole year. This indicates the relative amount of LFI cover for each month compared to the LFI cover of the whole year.

Figure 9Ice extent time series of AARI ice charts, FMI-A and FMI-B during the 1-year period from 1 November 2015 to 31 October 2016. The time series is weekly with FMI-A and FMI-B for the same days as the weekly AARI ice charts.

Figure 10FMI-A (a) and FMI-B (b) LFI time series for the whole study period from 15 October 2015 to 31 August 2017. Also the time series of Kara Sea subregions – southwestern (SW), northeastern (NE), and Gulf of Ob (Ob) – have been included. The division of Kara Sea into subregions (c).

Figure 11Temporal LFI coverage (percentage) during the period from 1 November 2015 to 31 October 2016 based on the weekly AARI ice charts (a), daily FMI-A (b) and daily FMI-B (c). The values (percentages) indicate the time fraction of the one-year period in which there was LFI at each grid cell.

The results of the comparison of FMI-A and FMI-B LFI to AARI ice chart LFI can be seen in Table 1. In the first column are the fractions (in percents) of the LFI classified correctly when compared to AARI ice chart grids for FMI-A and FMI-B, and in the second column are the relative numbers (with respect to the AARI ice chart LFI extent) of grid points, which are not LFI according to the AARI ice charts but still classified as LFI by the proposed algorithms. In the parentheses are the standard deviations over all the weekly cases included in the comparison. It can be seen that FMI-A is able to locate over 73 % of the LFI indicated by the AARI ice charts, and in addition over 20 % of additional LFI areas were suggested by FMI-A compared to the AARI LFI area. FMI-B only detects a little over half of the LFI suggested by the AARI ice charts, but very few areas outside the AARI ice chart LFI area are classified as LFI by FMI-B. An example of the LFI extent based on the cropped AARI ice chart of 8 March 2016 in Fig. 6 and FMI-A and FMI-B LFI estimates of the same day are shown in Fig. 7. It can be seen that basically AARI ice chart LFI and FMI-A cover the same areas, but there still are some differences near the boundaries of the detected LFI area. This kind of differences occurs in most cases, at least partly explaining the differences in classification rates in Table 1. The total LFI extent detected by FMI-A and LFI extent given by the AARI ice charts are similar. FMI-B detects significantly less LFI than present in the AARI ice charts, but still the LFI area locations agree well, just that the LFI area is smaller in the detection results of LFI-B than in the AARI ice charts.

Also monthly comparisons between the AARI ice chart LFI and FMI-A and FMI-B LFI were made. The results show that the FMI-A LFI estimates covered about 80 % or more of the AARI LFI during the winter months (January–April, November–December) and less (60–70 %) during the spring and summer months. Also the number of FMI-A false LFI detections was increased towards the summer (up to over 40 % of the AARI LFI cover in July). For FMI-B the number of false detections remained low for the whole year, but the relative number of FMI-B detections matching with AARI ice chart LFI also decreased towards summer and was very low in July. On the other hand the total amount of LFI in July was also low, and this does not have a large effect on the total classification percentage with respect to the AARI ice chart LFI. The monthly classification results and the relative amount of LFI (monthly fractions of total number of AARI ice chart LFI pixels during the 1-year period) are shown in Fig. 8.

For comparing the LFI extent evolution in time the weekly LFI extents over the whole study area during the 1-year period corresponding to the AARI ice charts used in this study were computed. These results can be seen in Fig. 9. The FMI-A LFI extent follows the AARI ice chart LFI extent quite well, having larger temporal variations. In the spring the FMI-A LFI extent first decreases faster (in April 2016) than the AARI LFI, but later in the melting period (in May 2016) the FMI-A decrease becomes slower compared to the AARI LFI extent. FMI-B systematically gives significantly smaller LFI extent estimates, approximately 70 % of the corresponding AARI and FMI-A LFI extent throughout the whole one-year period.

In Fig. 10 LFI extent time series for both FMI-A and FMI-B over the whole study period are shown. According to FMI-A the maximum LFI extent over the study area was around 170 000 km2 during the winter 2015–2016 and over 180 000 km2 during the winter 2016–2017. The LFI maximum in 2016–2017 was reached later than in 2015–2016. This can be partly explained based on the weather conditions making 2016–2017 a more severe ice winter and having a colder spring than 2015–2016. For the FMI-B LFI extent time series the LFI extent estimates are approximately 70 % of the FMI-A LFI extent, and the evolution of the time series is in general similar to that of FMI-A.

The LFI time series were also compared to air temperature measurements at Longyearbyen (see Fig. 1 for the location) weather station in Svalbard (78.22 N, 15.63 E) provided by Met Norway at http://www.yr.no (last access: 8 August 2018) and to the NCEP–NCAR numerical weather model reanalysis air temperature at two locations in the Kara Sea area, one near the Kara gate in the southern Kara Sea and another near the northern tip of the islands of Novaya Zemlya. The model reanalysis data were used because there were no weather station measurement data available over the Russian Arctic. The weather data indicated that the winter 2016–2017 was more severe than the winter 2015–2016 at all the three locations. At Longyearbyen the winter temperatures were milder than for the Kara Sea locations. As seen in Fig. 10 the LFI extent for the winter 2016–2017 was larger than for the winter 2015–2016. Even though the LFI extent can not be explained by the air temperature alone (Olasen2016), this comparison between the two winters is in agreement with the air temperature data.

The LFI extent of the subregions of southwestern Kara Sea, northeastern Kara Sea and Gulf of Ob are also shown in Fig. 10. The fast ice grows most rapidly in the Gulf of Ob and quite slowly in the southwestern Kara Sea during both 2015–2016 and 2016–2017. Also the LFI melt in the Gulf of Ob is fast when compared to the other two areas presented. This is probably due to the flowing water coming along the Ob River. These annual variations can be compared to those of Fig. 2 in .

Also the LFI extent temporal fraction (in percents) for FMI-A and FMI-B at each grid cell over the one-year period from November 2015 to October 2016 was computed in a similar manner as in . For comparison the corresponding fraction was computed also for the weekly AARI ice chart LFI extent of the same one-year time period. These numbers also indicate the annual duration of the LFI at each grid cell and are given as percentages of the one-year time period in Fig. 11. The results for the whole time period from October 2015 to August 2018 (not shown here) were quite similar, except that the percentages were higher because part of the summer period of 2017 (with no or very little LFI) was not present in the time series covering the whole study period. The results of the AARI ice chart LFI extent and FMI-A LFI extent were quite similar. In some areas there were minor differences, but in general AARI ice chart LFI fraction and FMI-A LFI fraction were in good agreement. On the other hand, FMI-B with the parametrization used here (optimal thresholds THH and THV) underestimated the LFI extent fraction compared to AARI ice chart LFI extent, but still the same LFI areas were captured, only with a shorter duration of LFI according to FMI-B.

5 Discussion and conclusions

In this study an algorithm for detecting LFI over a test area in the Kara and Barents seas using daily Sentinel-1 dual-polarized SAR mosaics was developed and tested. Both SAR channels (HH and HV) were used jointly in this study. Two versions of the algorithm were presented: FMI-A applies the optimal thresholds for SAR HH and HV channels and after some post-processing combines the channel-wise LFI estimates; in FMI-B an additional multi-temporal logical operation (logical AND) is performed to decrease the misclassifications to the LFI class at the expense of less detected LFI compared to the AARI ice chart LFI. FMI-B can be considered as an algorithm locating only the areas which very likely represent LFI. Daily LFI extent estimates for a period from October 2015 to August 2017 were generated. The results were also evaluated against weekly Russian AARI ice charts, and the correspondence was found to be at an acceptable level, especially when comparing the LFI extent time series. The ice extent over the study area given by the proposed algorithm FMI-A agrees quite well with the AARI ice chart ice extent. However, there exist some differences in the location of the LFI, especially near the detected LFI zone boundaries when compared to the AARI ice chart LFI. During the melting season the difference between AARI ice chart LFI and FMI-A LFI is larger than during the freeze-up and mid-winter periods. This can be seen in both the classification error and the ice extent time series. It should be noted here that AARI ice charts are typically based on satellite image analysis (SAR and optical–IR) of a few days prior to the assigning date of the ice chart, and the proposed algorithms use SAR data over a two-week period prior to the issuing date. Due to the different time spans and spatial resolutions of the input data sets, differences between the proposed LFI estimates and AARI ice chart LFI may appear.

In this study the optimal threshold based on a training set consisting of AARI ice chart LFI data was used for both FMI-A and FMI-B. During the winter months (November–April) the amount of correctly detected LFI compared to the AARI ice chart LFI was around 80 %, and the number of false detections was 20 % or less. In the melt period (May–July) the detection rates were worse. By using these settings FMI-B had a good performance in the sense that it makes very few false LFI detections compared to AARI ice chart LFI. However, then only a little over half of the total AARI LFI is detected by FMI-B. In this sense FMI-A performs significantly better. However, with lower values for the thresholds THH and THV FMI-B detects more AARI LFI at the expense of more false LFI detections. For example with the threshold values THH=0.19 and THV=0.15, 68.6 % of the AARI LFI was detected and 37.5 % of additional (to AARI) LFI was detected by FMI-B.

According to this study the proposed algorithm (FMI-A) is considered suitable for operational LFI detection to be included in the daily automated FMI sea ice products , which have thus far already been run in an operational test mode over the studied area during a few winters. There also exist plans at FMI to replace the TOPAZ-4 ice model data used as background information for ice thickness estimation from Earth observation (EO) data with the coarse-scale ice thickness from radar altimeter data and with the FMI thermodynamic ice model HIGHTSI over the static ice areas during the static ice time periods detected by the proposed LFI algorithm. For these reasons it is important to get the LFI information in a similar temporal and spatial resolution as the other sea ice products. The automated LFI detection also produces systematic LFI analyses which are not dependent on possible subjective interpretation or varying skills of different ice analysts producing the ice charts.

Use of temporal cross-correlation average and temporal cross-correlation median in the algorithm produced quite similar results, and because of its faster computation temporal cross-correlation average was selected here instead of temporal cross-correlation median (requiring sorting of the samples). The execution times on a single CPU core (Intel Xeon 2.5 GHz) with a sufficient amount of RAM memory were reasonable also for operational purposes: computation of LFI extent for one daily SAR mosaic takes 2–4 min. As the computation can easily be parallelized, LFI extent estimation, for example, for the whole Arctic or Antarctic areas can easily be performed in a reasonable time by dividing the workload to multiple CPU cores. Here a simple mask based on iteratively estimated distance from land was used to reduce the area of computation and thus fasten the algorithm execution. This proved to be a very useful feature in computation of longer time series; the execution time was reduced to less than half of the execution time without using the mask.

Compared to other LFI detection methods the proposed method has some advantages. The obvious advantage of using SAR data instead of radiometer data is the significantly higher resolution, and the advantage of using SAR data instead of optical or infrared–near-infrared satellite data, such as MODIS , is the ability of SAR to measure in all weather and lighting conditions independently of clouds or sunlight. LFI can be derived from ice drift based on multi-temporal SAR imagery (Karvonen2012), but estimation of the ice drift is a much more time-consuming process than applying direct temporal cross-correlation. The LFI estimation accuracy of methods based on SAR ice drift is approximately similar to that of LFI-A. Using temporal cross-correlation minimum instead of its average is less robust to local errors than a statistical measure, such as average or median, as it is based only on one value. Methods based on SAR segmentation and SAR backscattering have several potential error sources: C-band SAR backscattering is dependent on the ice surface roughness, which may vary for LFI; SAR backscattering is also dependent on the SAR incidence angle, which varies for different acquisitions of a fixed location; wet snow cover has a significant effect on SAR backscattering, making algorithms directly based on SAR backscattering unreliable, especially during the melting season.

An LFI product covering the whole Arctic and Antarctic based on Sentinel-1 is technically feasible. There is one limitation related to the current Sentinel-1 acquisition observation scenario: over most of the Arctic Sentinel-1 is acquiring EW mode HH polarization only and dual-polarized data are acquired only over the European Arctic and Greenland areas. However, it seems that even the HH channel Sentinel-1 data alone are sufficient for estimating the LFI extent, even though combining the two polarization channels would increase the reliability of the product to some extent. Some preliminary experiments indicated a slight increase of false LFI detections compared to AARI ice charts when using HH channel data alone. On the other hand, the amount of correctly detected LFI remained approximately the same as for the combined HH and HV channel classification. The major obstacle of establishing an operational pan-Arctic or Antarctic LFI service based on Sentinel-1 SAR imagery is the vast amount of daily Sentinel-1 data and the current limited data transmission and storage resources.

According to FMI-A there seemed to be LFI even during the summer (late August). The same areas were classified as LFI by FMI-A in both the summers included in this study. This summer LFI naturally represented a classification error over the study area. Those few areas indicated as LFI by FMI-A were typically areas very close to the coastline and thus very likely due to inaccuracies in positioning of the land mask, causing land or mixed land–sea pixels to be included in the temporal cross-correlation computation. To exclude these areas the LFI detected by FMI-A in late August 2016 was filtered out (subtracted) from all the FMI-A and FMI-B LFI extent maps.

Also, ways to further improve the current algorithms need to be studied. Some interesting alternatives for future algorithm development are the use of varying thresholds according to the time of the year or weather data as well as the application of a dual-threshold temporal cross-correlation average thresholding scheme (i.e., first applying a lower threshold, then applying a higher threshold and finally combining the two results in an optimal way). In addition, a combination of an application of FMI-B and FMI-A could be studied. This combination could first locate the areas representing LFI with a high likelihood (FMI-B) and then extend this initial LFI extent based on the FMI-A result adjacent to the initial LFI areas detected by FMI-B (a region growing method).

Data availability
Data availability.

The data are currently available for the SPICES project partners and for other parties for request. We will study the possibility of providing the data through public data repositories later. Currently the LFI data can only be accessed by contacting the author (except for the SPICES project partners, who have direct access to the FMI FTP site). Future plans include continuing to compute a time series of daily LFI extent over the study area and to update the LFI data set twice annually, once in spring and once in autumn. The data will be available for interested parties by request on the FMI FTP site in GeoTIFF (thematic map) and NetCDF (numeric data) formats. The Sentinel-1 SAR data are available through the ESA Copernicus Science Hub: https://scihub.copernicus.eu/.

Competing interests
Competing interests.

The author declares that there is no conflict of interest.

Acknowledgements
Acknowledgements.

The author would like to thank the editor and the reviewers for the constructive comments and suggestions provided. The work was supported by the project space-borne observations for detecting and forecasting sea ice cover extremes (SPICES) funded by the European Union's Horizon 2020 Programme (grant agreement no. 640161).

Edited by: Christian Haas
Reviewed by: two anonymous referees

References

Agnew, T. A., Le, H., and Hirose, T.: Estimation of large scale sea ice motion from SSM/I 85.5 GHz imagery, Ann. Glaciol., 25, 305–311, 1997. a

Antonova, S.: Spatial and temporal variability of the fast ice in the Russian Arctic, Master thesis, State University of St. Petersburg, Russia and University of Hamburg, Germany, 2011. a

Barry, R. G., Moritz, R. E., and Rogers, J. C.: The fast ice regimes of the Beaufort and Chucksi Sea coasts, Alaska, Cold Reg. Sci. Technol., 1, 129–152, 1979. a

Cheng, B., Vihma, T., and Launiainen, J.: Modelling of the superimposed ice formation and subsurface melting in the Baltic Sea, Geophysica, 39, 31–50, 2003. a

Divine, D., Korsnes, R., and Makshtas, A.: Variability and climate sensitivity of fast ice extent in the north-eastern Kara sea, Polar Res., 22, 27–34, 2003. a

Divine, D., Korsnes, R., and Makshtas, A. P.: Temporal and spatial variation of shore-fast ice in the Kara Sea, Cont. Shelf Res., 24, 1717–1736, https://doi.org/10.1016/j.csr.2004.05.010, 2004. a, b

Eicken, H., Dmitrenko, I., Tyshko, K., Darovskikh, A., Dierking, W., Blahak, U., Groves, J., and Kassens, H.: Zonation of the Laptev Sea landfast ice cover and its importance in a frozen estuary, Global Planet. Change, 48, 55–83, 2005. a, b

Fily, M. and Rothrock, D. A.: Sea ice tracking by nested correlations, IEEE T. Geosci. Remote, GE-25, 570–580, 1987. a

Fraser, A. D., Massom, R. A., and Michael, K. J.: Generation of high-resolution East Antarctic landfast sea-ice maps from cloud-free MODIS satellite composite imagery, Remote Sens. Environ., 114, 2888–2896, 2011. a, b, c

Fraser, A. D., Massom, R. A., Michael, K. J., Galton-Fenzi, B. K., and Lieser, J. L.: East Antarctic Landfast Sea Ice Distribution and Variability, 2000–08, J. Climate, 25, 1137–1156, 2012. a

Hearn, D. and Baker, M. P.: Computer Graphics, C version, Prentice Hall Press, Upper Saddle River, New Jersey, USA, p. 130, 1997. a

JCOMM (Joint World Meteorological Organization (WMO) – Intergovernmental Oceanographic Commission (IOC) Technical Commission for Oceanography and Marine Meteorology), SIGRID-3: A vector archicve format for sea ice charts, JCOMM-TR-023, revision 3, available at: https://www.jcomm.info/index.php?option=com_oe&task=viewDocumentRecord&docID=4439 (last access: 8 August 2018), 2014. a

Kalnay, E., Kanamitsu, M., Kistler, R., Collins, W., Deaven, D., Gandin, L., Iredell, M., Saha, S., White, G., Woollen, J., Zhu, Y., Chelliah, M., Ebisuzaki, W., Higgins, W., Janowiak, J., Mo, K. C., Ropelewski, C., Wang, J., Leetmaa, A., Reynolds, A., Jenne, R., and Joseph, D.: The NCEP/NCAR 40-Year Reanalysis Project, B. Am. Meteorol. Soc., 77, 437–470, https://doi.org/10.1175/1520-0477(1996)077<0437:TNYRP>2.0.CO;2, 1996. a

Karvonen, J.: Operational SAR-based sea ice drift monitoring over the Baltic Sea, Ocean Sci., 8, 473–483, https://doi.org/10.5194/os-8-473-2012, 2012. a, b

Karvonen, J.: Baltic Sea Ice Concentration Estimation Based on C-Band Dual-Polarized SAR Data, IEEE T. Geosci. Remote, 52, 5558–5566, https://doi.org/10.1109/TGRS.2013.2290331, 2014. a

Karvonen, J.: Baltic Sea Ice Concentration Estimation Using SENTINEL-1 SAR and AMSR2 Microwave Radiometer Data, IEEE T. Geosci. Remote, 55, 2871–2883, https://doi.org/10.1109/TGRS.2017.2655567, 2017. a

Kim, M., Im, J., Han, H., Kim, J., Lee, S., and Shin, M.: Landfast sea ice monitoring using multisensor fusion in the Antarctic, GISci. Remote Sens., 52, 239–256, 2015. a

Kwok, R., Schweiger, A., Rothrock, D. A., Pang, S., and Kottmeier, C.: Sea ice motion from satellite passive microwave imagery assess with ERS SAR and buoy motions, J. Geophys. Res., 103, 8191–8214, 1998. a

Launiainen, J. and Cheng, B.: Modelling of ice thermodynamics in natural water bodies, Cold Reg. Sci. Tech., 27, 153–178, 1998. a

Lepparanta, M.: The Drift of Sea Ice, 2nd edn., Springer-Verlag, Berlin-Heidelberg, Germany, 2011. a, b

Mahoney, A., Eicken, H., Graves, A., Shapiro, L., and Cotter, P.: Landfast sea ice extent and variability in the Alaskan Arctic derived from SAR imagery, Proc. IEEE International Geoscience and Remote Sensing Symposium Proceedings (IGARSS'04), 3, 2146–2149, 2004. a

Mahoney, A., Eicken, H., Shapiro, L., and Graves, A.: Defining and locating the seaward landfast ice edge in northern Alaska, 18th Proc. International Conference on Port and Ocean Engineering under Arctic Conditions (POAC 2005), Potsdam, NY, 26–30 June, 991–1000, 2005. a, b

Mahoney, A., Eicken, H., Gaylord, A. G., and Shapiro, L.: Alaska landfast sea ice: Links with bathymetry and atmospheric circulation, J. Geophys. Res., 112, 2156–2202, https://doi.org/10.1029/2006JC003559, 2007. a

Mahoney, A. R., Eicken, H., Gaylord, A. G., and Gens, R.: Landfast sea ice extent in the Chukchi and Beaufort seas: The annual cycle and decadal variability, Cold Reg. Sci. Technol., 103, 41–56, https://doi.org/10.1016/j.coldregions.2014.03.003, 2014. a

Makynen, M. and Karvonen, J.: MODIS Sea Ice Thickness and Open Water–Sea Ice Charts over the Barents and Kara Seas for Development and Validation of Sea Ice Products from Microwave Sensor Data, Remote Sens., 9, 1324, https://doi.org/10.3390/rs9121324, 2017. a, b

Marbouti, M., Praks, J., Antropov, O., Rinne, E., and Lepparanta, M.: A Study of Landfast Ice with Sentinel-1 Repeat-Pass Interferometry over the Baltic Sea, Remote Sens., 9, 833, https://doi.org/10.3390/rs9080833, 2017. a

Meyer, F. J., Mahoney, A. R., Eicken, H., Denny, C. L., Druckenmiller, H. C., and Hendricks, S.: Mapping arctic landfast ice extent using L-band synthetic aperture radar interferometry, Remote Sens. Environ., 115, 3029–3043, 2011. a

Morales Maqueda, M. A., Willmott, A. J., and Biggs, N. R. T.: Polynya Dynamics: a Review of Observations and Modeling, Rev. Geophys., 42, 1944–9208, https://doi.org/10.1029/2002RG000116, 2004. a

Olasen, E.: A dynamical model of Kara Sea land-fast ice, J. Geophys. Res.-Oceans, 121, 3141–3158, https://doi.org/10.1002/2016JC011638, 2016. a

Polyakov, I. V., Alekseev, G. V., Bekryaev, R. V., Bhatt, U. S., Colony, R., Johnson, M. A., Karklin, V. P., Walsh, D., and Yulin, A. V.: Long-term ice variability in Arctic marginal seas, J. Climate, 16, 2078–2085, https://doi.org/10.1175/1520-0442(2003)016<2078:Liviam>2.0.CO;2, 2003. a

Polyakov, I. V., Walsh, J. E., and Kwok, R.: Recent changes of Arctic multiyear sea ice coverage and the likely causes, B. Am. Meteorol. Soc., 93, 145–151, https://doi.org/10.1175/Bams-D-11-00070.1, 2012. a

Sakov, P., Counillon, F., Bertino, L., Lisæter, K. A., Oke, P. R., and Korablev, A.: TOPAZ4: an ocean-sea ice data assimilation system for the North Atlantic and Arctic, Ocean Sci., 8, 633–656, https://doi.org/10.5194/os-8-633-2012, 2012. a

Selyuzhenok, V.: Validation of the satellite-based landfast ice mapping, Master thesis, State University of St. Petersburg, Russia and University of Hamburg, Germany, 2011. a, b

Selyuzhenok, V., Krumpen, T., Mahoney, A., Janout, M., and Gerdes, R.: Seasonal and interannual variability of fast ice extent in the southeastern Laptev Sea between 1999 and 2013, J. Geophys. Res., 120, 7791–7805, https://doi.org/10.1002/2015JC011135, 2015. a

Simila, M., Makynen, M., Karvonen, J., Gegiuc, A., and Gierisch, A.: Modeled Sea Ice Thickness Enhanced by Remote Sensing Data, Proc. ESA Living Planet Symposium, Prague, Czech Republic, 9–13 May 2016. a, b

Solomon, S. M., Manson, G., Monita, D., Hirose, T., and Power, D.: Synthetic Aperture Radar Remote Sensing of Bottom Fast ice in the MacKenzie Delta Region, Northwest Territories, Canada, 2005 ArcticNet Annual Conference Proceedings, 96–97, 2005. a, b

Spreen, G., Kaleschke, L., and Heygster, G.: Sea Ice Remote Sensing Using AMSR-E 89 GHz Channels, J. Geophys. Res., 113, C02S03, https://doi.org/10.1029/2005JC003384, 2008. a

Stringer, W. J., Barrett, S. A., and Schreurs, L.: Morphology of the Beaufort, Chukchi and Bering Seas nearshore ice conditions by means of satellite and aerial remote sensing: final report, Research unit 257, Geophysical Institute, University of Alaska Fairbanks, Fairbanks, Alaska, 1978. a

Stringer, W. J., Barrett, S. A., and Schreurs, L. K.: Nearshore Ice Conditions and Hazards in the Beaufort, Chukchi and Bering Seas, Report of Geophysical Institute, University of Alaska, Fairbanks, AK, USA, 130 pp., 1980. a

Sun, Y.: Automatic ice motion retrieval from ERS-1 SAR images using the optical flow method, Int. J. Remote Sens., 17, 2059–2087, 1996. a

Thomas, M., Geiger, C. A., and Kambhamettu, C.: High resolution (400 m) motion characterization of sea ice using ERS-1 SAR imagery, Cold Reg. Sci. Technol., 52, 207–223, 2008. a

Weeks, W. F.: On Sea Ice, University of Alaska Press, Fairbanks, Alaska, USA, 2010. a

Wessel, P. and Smith, W. H. F.: A Global Self-consistent, Hierarchical, High-resolution Shoreline Database, J. Geophys. Res., 101, 8741–8743, https://doi.org/10.1029/96JB00104, 1996.  a

JCOMM: WMO Sea-Ice Nomenclature I–III, World Meteorological Organization, Report No. 259, available at: http://www.jcomm.info/index.php?option=com_oe&task=viewDocumentRecord&docID=14598 (last access: 8 August 2018), 2015. a, b, c

Yu, Y. L., Stern, H., Fowler, C., Fetterer, F., and Maslanik, J.: Interannual variability of Arctic landfast ice between 1976 and 2007, J. Climate, 27, 227–243, https://doi.org/10.1175/JCLI-D-13-00178.1, 2014. a, b

Zubov, N. N.: Arctic Ice, translated from the Russian original “Ledy Arktiki” (Moscow, 1945), U.S Navy Electronics Laboratory, 1960. a