A baseline evaluation of oceanographic and sea ice conditions in the Hudson Bay Complex during 2016–2018 Open Access

In a companion paper (Lukovich et al., 2021), we examined atmospheric and river discharge conditions in the Hudson Bay Complex (HBC) from 2016 to 2018 relative to the 1981–2010 climatology as “input” to the Arctic and Northern Hemisphere Atlantic configuration of the Nucleus for European Modelling of the Ocean (NEMO)/LIM2 ice-ocean model and the Hudson Bay System Study (BaySys). In this additional baseline study, we examine oceanographic and sea ice conditions for the same time frame, as output from the NEMO model used by all BaySys teams, to provide an understanding and estimate of changes in physical and biogeochemical processes in response to relative climate change and impacts of the regulation of river discharge. Also presented in this study is the development of an integrated observational/modeling framework based on Lagrangian dispersion statistics to characterize sea ice dynamics in the HBC.

The HBC receives water from the Canadian rivers in its watershed and, as their link to the ocean, allows for examination of freshwater-marine coupling. Arctic water enters the HBC via Hudson Strait, as well as Fury and Hecla Strait, and exits via Hudson Strait. Intrusion of Arctic water enables a transfer of Arctic conditions to lower latitudes (Ingram and Prinsenberg, 1998). Freshwater and heat budgets are central to an understanding of changes in Hudson Bay (HB), with water mass balance determined by input from Arctic waters, river discharge, and sea ice melt (Prinsenberg, 1984; Ingram and Prinsenberg, 1998; St-Laurent et al., 2012; Carmack et al., 2016). In the present study, we examine sea surface temperatures (SSTs) integral to understanding the heat budget in HB, in addition to sea ice conditions and drift in particular that contributes to thickness and freshwater redistribution (Prinsenberg, 1988) through deformation processes, with implications for ice hazard assessments, forecasting, and resilience planning.

Previous studies have documented and evaluated observed and simulated oceanographic and sea ice conditions in the HBC (Danielson, 1971; Prinsenberg, 1986a, 1986b; Ingram and Prinsenberg, 1998; Saucier et al., 2004; Stewart and Lockhart, 2005; Hochheim and Barber, 2010; Hochheim et al., 2011; Landy et al., 2017; Jafarikhasragh et al., 2019, Ridenour et al., 2019). Prinsenberg (1986a) showed that surface temperature and salinity in the HBC increase with distance from the shoreline. Temperature (T) increases due to upwelling associated with northwesterly winds, while salinity (S) increases due to reduced impact from runoff further from shore. Regional variability in T and S (as well as sea ice variables including sea ice concentration (SIC), thickness, and drift) provides motivation for a basin-wide assessment such as is addressed by BaySys. Surface circulation in the HBC is characterized by cyclonic circulation in summer with weak coastal currents, dominant Coriolis effects, and density stratification (Prinsenberg, 1986b). Volume transport is driven by northwesterly winds in fall, and density-driven currents in response to runoff and ice melt in summer. Prinsenberg and Freeman (1986) also documented a weak diurnal signal that loses amplitude and strength with cyclonic circulation in the HB complex. Recent studies, however, have demonstrated the existence of easterly currents in southwestern HB in an anticyclonic/cyclonic configuration attributed to the combined effects of changes in seasonal river discharge associated with regulation and anticyclonic surface winds (Ridenour et al., 2019).

Previous modeling studies of sea ice dynamics in HB demonstrated that sea ice growth rates in winter are governed by ice drift and deformation in southern HB, with seasonal variations in sea ice state and dynamics and enhanced ridging in winter within a regime of high ice concentration and thickness (Saucier et al., 2004; Jafarikhasragh et al., 2019). Sea ice begins to form in northwestern HB, where it is transported to southeastern HB (Markham, 1981; Prinsenberg, 1988). Thickness distributions are due to motion of the pack ice, with ice drift speeds on the order of 10 cm/s in northwest HB and 1 cm/s in southeast HB (Stewart and Lockhart, 2005). Northwesterly winds and tidal mixing give rise to polynya formation in northwestern HB. Maximum ice cover exists in April and May, and maximum thicknesses can range from 71 cm (Moosonee) to 285 cm (Inukjuak) between February and June (Stewart and Lockhart, 2005). Also central to the HB system is the formation of landfast ice that influences freshwater-marine coupling and communication between nearshore and offshore processes. Leads form along fast ice edges with offshore winds. In mid-July, ice is no longer considered a hazard. Hochheim and Barber (2010) showed that fall freeze-up/sea ice formation begins near Week 45 until complete ice coverage, exceeding 20%–30%, in Week 48; spring breakup occurs near Week 23, with variability between years due to differences in summer and autumn winds, air temperature, cloud cover, and snow cover (Hochheim et al., 2011). Also highlighted in both studies was east–west asymmetry in SIC anomalies associated with surface winds. The importance of sea ice dynamics to the freshwater budget is illustrated by Prinsenberg (1988), who showed that an underestimation in offshore ice volume can be attributed to freshwater stored in ice ridges that can increase freshwater contributions by as much as 30%. In addition, because the magnitude of density-driven currents is proportional to the runoff rate, Prinsenberg (1983) noted that hydroelectric developments that increase winter runoff will also increase winter circulation.

In this baseline study, we examine sea ice and oceanographic conditions during the BaySys time frame using reanalysis products. In an Eulerian analysis, sea ice area (SIA), drift speed, and meridional circulation index (MCI), as defined in the next section, are evaluated for the 2016–2018 BaySys time frame relative to the 1981–2010 climatology. In a Lagrangian analysis, sea ice deformation, computed from sea ice beacons deployed near Churchill in February 2017, is examined for the impacts of March 2017 storm, characterized in Lukovich et al. (2021) by strong winds locally and high levels of precipitation regionally, based on the spatial and temporal evolution in triangular arrays.

Study objectives were thus to compare oceanographic and sea ice conditions for 2016–2018 relative to the 1981–2010 climatology and to examine the impact of the blizzard/extreme storm on sea ice dynamics in 2017 as a case study. We used standard anomaly maps, as in the companion paper on baseline atmospheric conditions (Lukovich et al., 2021), to assess spatial variability in SST and ice conditions relative to the 1981–2010 climatology (or 1982–2010 in the case of SST). Temporal changes are captured by monthly plots, while rankings depict extremes associated with SICs and drift. Definitions and methods are presented in Section 2; temporal and spatial variability in SSTs, sea ice state and dynamics in Section 3.1; and rankings in Section 3.2. The case study for the March 2017 blizzard is presented in Section 3.3, as an example of an extreme event which, in a storylines approach to describing possible future pathways and scenarios based on an assessment of a range in plausible outcomes and compound extreme events including windstorms with heavy precipitation (Shepherd et al., 2018), is relevant to climate change impact considerations and planning.

For this study, as in the companion study (Lukovich et al., 2021), the 1981–2010 time frame was selected because it (i) falls after the establishment of river discharge regulation and (ii) coincides with a climatological and conventional normal time interval established by Environment and Climate Change Canada (2020). Variables examined (and selected based on available observational and reanalysis data) include SST, SIC, and sea ice drift. Sea ice beacon observations from the BaySys field campaign were analyzed using Lagrangian dispersion statistics, including displacements in individual beacons and evolution in triangular configurations selected from an array of beacons deployed off the coast of Churchill during the 2017 winter BaySys field campaign.

To study SST in the HBC over the baseline period (2016–2018), SST from satellite was compared with its climatology (1982–2010). We used satellite data from the Optimum Interpolation SST (OISST) Version 2 data set (Reynolds et al., 2007), which is available from the National Oceanic and Atmospheric Administration (NOAA) Earth System Research Laboratory Physical Science Division (Banzon et al., 2016). The data are available from 1982 until now, which is why the SST analysis starts in 1982. The OISST data set has been used in many climatological and modeling studies (e.g., De Szoeke and Xie, 2008; Artale et al., 2010; Singh et al., 2013; Banzon et al., 2016) due to its good temporal and spatial coverage. These are daily SST records (one daily value for each pixel), with spatial resolution of 0.25° × 0.25° (approximately 25 km) based on the combination of two passive satellite data set, the Advanced Very High-Resolution Radiometer infrared satellite and Advanced Microwave Scanning Radiometer on the Earth Observing System, supplemented with SST observations from ships and buoys. Changes and bias corrections, applied to all data since the beginning of production in Version 2 of the OISST data product (as described in Banzon et al., 2016) used in the present analysis, ensure consistency in comparison between the BaySys time frame years and historical climatology.

SIC data come from the NOAA/National Snow and Ice Data Center (NSIDC) Climate Data Record of Passive Microwave Sea Ice Concentration, Version 3 (Meier et al., 2017). This data set covers the period of 1981–1987 every other day and is daily for the 1988–2018 period. The average of 2 consecutive days was used for the day missing between 2 days. Moreover, the First of March was considered as the first day of the year. The NSIDC Version 4 of the sea ice drift product (Tschudi et al., 2019) was also used in this analysis. Although the NSIDC ice drift product (25-km spatial resolution) excludes Hudson Strait and James Bay, as does the medium-resolution OSISAF ice drift product (62.5-km spatial resolution), the former provides data from 1979 to the present, whereas the latter provides data from 2006 onward. To enable comparisons for the same time frame as in the present analysis (i.e., 1981–2018), the NSIDC sea ice drift product was used. Lagrangian sea ice drift data from beacons deployed in February 2017 were further analyzed to characterize sea ice drift and deformation based on beacon triplets (following Lukovich et al., 2015; Lukovich et al., 2017), and the blizzard/extreme event in particular. Five of the 25 beacons deployed off the coast of Churchill were examined, as these instruments provided data prior to, during, and following the March 2017 storm.

Sea ice freeze-up and breakup dates in the HBC were determined according to diagnostics and criteria described in Peng et al. (2018). Day of advance is defined as the first day that SIC increases above 15% after the last summer minimum; day of closing, as the first day that SIC increases about 80% after the last summer minimum; day of opening, as the last day SIC drops below 80% before the first summer minimum; and day of retreat, as the last day that SIC drops below 15% before the first summer minimum.

Standardized monthly anomalies were computed using the technique described in Lukovich et al. (2021, their Section 2) and equations provided in the Supplemental Material to illustrate spatial variability in sea ice conditions during the 2016–2018 BaySys time frame. The region of interest encompasses 50º–70ºN and 95º–75ºW (Figure 1). SIA was computed as the sum of grid cells exceeding 15% SIC (following the NSIDC convention defining 15% as the threshold between ice-covered and ice-free regions) multiplied by the SIC at each grid cell. From the NSIDC zonal (u) and meridional (v) sea ice drift components, sea ice drift speed and the MCI were analyzed as described in Francis and Vavrus (2015) and defined as

to characterize changes in relative zonal and meridional sea ice drift. Predominantly zonal sea ice drift is depicted by values approaching zero, while predominantly meridional sea ice drift is depicted by values approaching positive or negative one.

A key objective of the BaySys project was to develop an integrated observational-modeling framework for the HBC. In addition to traditional characterizations associated with model-observational data evaluation, including time series, maps of means and standard deviations, trends, and process studies that enable comparison between model output and satellite and in situ observations from an Eulerian perspective, of interest in this study are sea ice dynamics from a Lagrangian perspective that depicts the ability of models to capture sea ice dispersion characteristics relevant for tracer and pollutant transport and mixing characterization, forecasting, and prediction. Here and in Section 3.3, we present the framework for such an evaluation using observational data for a case study of an extreme event during the BaySys field program, as a template for ongoing Lagrangian dispersion studies focused on discerning the ability of sea ice models to capture sea ice dynamics over a range of spatial and temporal scales.

In this study, we analyzed Lagrangian dispersion statistics using measurements from ice beacons deployed during the BaySys field campaigns, as outlined in Lukovich et al. (2011, 2015, 2017). Examined in particular is single-particle dispersion defined as

for x_i, the zonal and meridional location of the ith particle/beacon in the ensemble as a function of elapsed time, t; angle brackets denote ensemble averaging. Regional-scale circulation is characterized by the scaling exponent α according to the relation

where α = 2 corresponds to a ballistic regime indicative of advection, α = 1 to a diffusive regime, α = 5/3 to an elliptic regime, α = 5/4 to a hyperbolic regime, and α < 1 to a subdiffusive or “trapping” regime. Single-particle dispersion was used in particular to evaluate the displacement of individual ice parcels and regional-scale structure in the sea ice drift field prior to, during, and following the March blizzard of 2017. As noted in previous studies, a ballistic dispersion regime depicts advection associated with organized structure in the ice drift field, a diffusive regime captures the behavior of particles (beacons or ice floes) that follow independent random walks, and a subdiffusive regime characterizes trapping such as would occur with dominant contributions from ice–ice interactions. A strong rotational component in the ice drift field is captured by an elliptic regime, whereas strain (shear and stretching)-dominated flow is captured by a hyperbolic regime associated with along-shear transport. Temporal scaling maps depict scaling exponent values along ice beacon trajectories for the time frame considered.

Three-particle dispersion (Prinsenberg et al., 1998; Hutchings et al., 2011; Lukovich et al., 2017) was evaluated according to the time rate of change in triplet area, A, to compute sea ice divergence, $D=1AdAdt=∂u∂x+∂v∂y,$ vorticity, $V=1A′dA′dt,$ shear, $S=1A″dA″dt,$ and the stretching deformation rate, $N=1A‴dA‴dt,$ where primes indicate a 90° clockwise rotation in velocity vectors. Divergence depicts changes in triangle area, vorticity in triangle orientation, and changes in shearing and stretching rates in the triangular area and shape due to distortion in the sea ice cover. Changes in sea ice motion gradients were further characterized by relative differential kinematic parameters (DKPs), including the total deformation D² + S² + N², vorticity squared, and the Okubo–Weiss criterion $OW=Re14D2+S2+N2−V2+DS2+N2−V2,$ which monitors relative contributions from deformation due to distortion in the sea ice cover OW > 0, and vorticity in response to winds and inertial oscillations OW < 0. These diagnostics were used to examine sea ice deformation prior to, during, and following the March 2017 storm as a case study in an extreme event and to improve our understanding (and, in future, model representation) of sea ice deformation response to extreme events.

Monthly plots of mean (spatially averaged over the HBC) standardized anomalies for SSTs, SIA, drift speed, and MCI illustrate temporal variability for the 1981–2018 time frame and differences between years during the 2016–2018 BaySys time frame. In the following, monthly plots and time series for sea ice drift speed and MCI are weighted, scaled by the number of ice-covered grid cells.

Monthly plots of SST standardized anomalies show warmer SSTs in October, November, and December from 2016 to 2018 relative to the 1982–2010 climatology (Figure 2). Noteworthy are sustained warmer temperatures from January to April in 2016, throughout the annual cycle in 2017, and cooler SSTs from January to September in 2018.

Maps of the 2016 monthly SST standardized anomaly relative to 1982–2010 climatology show that the maximum anomaly occurred in northern HB from May to August, while the pattern changed toward the west and center of HB during November and December (Figure S1A). This positive SST standardized anomaly represents warmer temperatures in these regions compared to its climatological value. In 2017, positive anomalies were observed around the south shores of HB in January, February, March, and April (Figure S1B). Moreover, the maximum positive anomaly occurred in July and June in the north and south of HB. Contrary to 2016 and 2017, the HBC in 2018 experienced predominantly weak or negative SST standardized anomalies, apart from a positive anomaly in June over the west side of the HB (Figure S1C). Overall, SSTs in 2016 and 2017 were warmer than in 2018 and the 1982–2010 climatology period in those particular regions.

Time series of SSTs and SST standardized anomalies further demonstrate warmer SSTs in 2017 and to a lesser extent in 2016 relative to cooler SSTs in 2018 comparable to the 1982–2010 climatology (Figure 3). Warmer SSTs were observed throughout the annual cycle in 2017.

Monthly plots of standardized anomalies for SIA show a decline characteristic of a more heterogeneous sea ice cover in early winter over the past several decades (Figure 4). Similar plots for ice-covered fraction (defined as the ratio in the ice-covered to total number of grid cells) demonstrate enhanced variability and reduced ice coverage during the transition months of June and November (Figure 5) for the entire time frame. Predominantly negative SIA standardized anomalies characterize 2016 and the full annual cycle in 2017, while positive SIA standardized anomalies characterize the winter months in 2018 (Figure 4). Enhanced (reduced) mean drift speed is observed in December (January) for 2016, 2017, and 2018 (Figure 6). Weakened meridional sea ice circulation characterizes December 2016 and 2018 (Figure 7). Contrasting MCI anomalies in May of 2016 and 2017, as well as in January and to a lesser extent December of 2017 and 2018, also reflect the contrasting sea level pressure (SLP) anomalies during the BaySys time frame (Lukovich et al., 2021, their figure 1).

Higher SIA standardized anomalies despite warmer SSTs in October, November, and December (Figures 2 and 4) can be attributed to early ice advance (as is shown below) due to colder surface air temperatures in September, October, and November of 2018 (Lukovich et al., 2021, their figure 16). Larger SIA standardized anomalies for January, February, and March of 2018 can be attributed, however, to cooler than normal SSTs (Figures 2 and 4).

Maps of standardized anomalies for monthly SIC further demonstrate regional differences in SIC during the 2016–2018 BaySys time frame (Figure S2A–C). Northwest HB is characterized in all 3 years by unusually high SIC in February; and in 2017 (2016 and 2018) by low (high) SIC in March relative to the 1981–2010 climatology. Comparatively high SIC was also observed in eastern HB in April and May of 2016 and 2018. Anomalously low SIC occurred throughout the basin from July to December of 2016 and in northwestern HBC in particular in November. In 2017, anomalously low SIC occurred throughout the HBC in January, March, and June to August; in 2018, in western HBC in a manner consistent with high SSTs in June.

Figure 8 shows the month when sea ice started to decrease and SIC dropped below 80% based on day of opening. The climatology map shows that sea ice started to open in May in the north and east of HB and north of Hudson Strait prior to the opening in the southwest and center of Foxe Basin, which tended to occur in late June. In general, the baseline years 2016–2018 follow the same pattern as the 1981–2010 climatology except in the east of HB in 2018 when, in contrast to other years, the ice started to break up later than in western HB. This later breakup is in keeping with the unusually high SIA in February of 2018 (Figure 4). The same regimes and patterns for day of opening also pertain to sea ice retreat (Figure S3). SIC started to decrease below 15% sooner over the north and west of HB in the climatology and in all baseline years except in eastern HB in 2018.

SIC for the 1981–2010 climatology started to increase and exceed the 15% threshold in late September and October in Foxe Basin and in late October and early November in northwest HB (Figure 9). This pattern is similar for all years, although the time for sea ice advance happens later in 2016 (early December). The pattern for sea ice closing (when SIC exceeds the 80% threshold) is consistent with that for sea ice advance (Figure S4). Sea ice started to close in late November. Again, this time is later for 2016 (late December).

Maps of standardized anomalies for monthly sea ice drift speed highlight regional variability in sea ice dynamics during the BaySys time frame (Figure S5A–C). In 2016, enhanced drift was observed adjacent to regions with unusually low SICs, including in western HBC in February and April, southeastern HBC in June, and northern HBC in December (Figure S5A). In 2017, enhanced sea ice drift speeds are found in lower SIC regimes in southeastern HBC in March, as well as northwestern HBC in April and November. Higher ice drift speed and SIC in northwestern HBC in December coincide spatially with gradients in anomalous SLP high and low regimes (Lukovich et al., 2021, their figure S1B, last panel) that would contribute to ice advection in this region (Figure S5B). In 2018, high ice drift speed anomalies in western HB in February and May are found in the vicinity of anomalously low SIC regimes (Figure S5C) during anomalously low SLP and windy atmospheric conditions (Lukovich et al., 2021, their figure 16).

Noteworthy are unusually high ice drift speeds in the HBC in March and April 2017 when unusually high river discharge occurred (Figure S5B; Lukovich et al., 2021, their figure S9). High ice drift speeds were also observed in February and April 2016 during a year characterized by high discharge in January and March. These results are consistent with the study by Prinsenberg (1983) showing enhanced sea ice circulation in response to increased runoff from hydroelectric developments in winter.

Standardized anomalies for the absolute value of the MCI as a measure of changes in meridional circulation in the HBC further highlight regional differences in circulation from 2016 to 2018 (Figure S6A–C). In this figure, enhanced (reduced) meridional circulation is depicted by positive (negative) anomaly values. In 2016, meridional circulation was enhanced in a lower SIC and higher sea ice drift regime in March and reduced in December characteristic of predominantly zonal flow. Similar behavior is observed in 2018, while the opposite occurred in 2017.

Time series of sea ice breakup and freeze-up, SIA, drift speed, and MCI with their standardized anomalies further demonstrate differences between years during the 2016–2018 time frame (Figures 10–13). To identify precise spatially averaged dates associated with the sea ice breakup and freeze-up patterns in Figures 8 and 9, the time series of days of opening, retreat, advance and closing are shown in Figure 10. The minimum SIC (day of retreat) happened earlier for baseline years of 2016 (Day 235) and 2017 (Day 242) compared with climatology (Day 244). Also, sea ice started to increase above 15% (day of advance) later for these years (Days 288 and 276, respectively) compared to climatology (Day 274). Year 2018 shows dates for sea ice retreat and advance that are similar to climatology.

Lower than normal (relative to the 1981–2010 climatology) SIA values are observed during spring months of 2016, with enhanced variability defined according to maximum and minimum SIA during the 1981–2018 time frame observed during spring and early winter (Figure 11). Anomalously high SIA is observed in 2018. Standardized anomalies for sea ice drift speed show lagged extrema in winter and high ice drift speeds in March of 2017 relative to 2016 and 2018 (Figure 12). Also of interest are low ice drift speeds due to low ice cover in November 2016 that yield standardized anomaly results comparable to 2017 and 2018. Time series for the MCI show enhanced meridional circulation in December 2017 compared to 2016 and 2018. Mean meridional sea ice circulation was enhanced in March during the extreme blizzard event and suppressed in April of 2017 following that storm (Figure 13).

In summary, 2016 was an unusually warm year (relative to the 1981–2010 climatology), with lower than normal SIA during winter, as well as higher (lower) than normal freshwater discharge to the HBC in winter (summer) months. In addition, 2018 was a predominantly cold and windy year, with higher than normal SIA in January and February, as well as low discharge to the HBC in May and June and from September to December. Furthermore, 2017 was characterized by a low in SLP and highs in temperature and precipitation in January and intermittent high and low wind events compared to the 1981–2010 climatology, with lower than normal SIA, unusually high zonal ice drift in April, as well as unusually high discharge in March and April and low discharge (high meridional ice drift) to the HBC in September.

Ranking the sea ice variables of SIA, drift speed, and MCI, spatially averaged over the HBC for the 1981–2018 time frame, highlights whether a particular month or season during the BaySys baseline 2016–2018 time frame is characterized by extreme sea ice conditions (Figures 14 and 15). Both figures provide a synopsis of the monthly plots presented in the previous section.

Rankings show that the HBC is characterized by low SIA during the winter months (December–February) of 2016–2017, which was partially restored in 2017–2018. High ice drift speeds are observed in December of 2016, 2017, and 2018, with enhanced meridional circulation observed in December of 2017. In consideration of only extreme events (Figure 15), low (high) SIA is observed in winter 2016/2017 (2017/2018), while low SIA coincides with high SLP regimes in fall/late summer in 2016 and 2017. High ice drift speeds coincide with strong winds in April of 2016; low (high) ice drift speeds are found in February (April) of 2017, which may be attributed to low SIA following the March blizzard and high SSTs in March and April. Low ice drift speeds occurred following unusually high SIA in winter of 2018, while high ice drift speeds coincided with windy conditions in May and August of 2018. Rankings also show weakened meridional circulation in April of 2017 following the March 2017 blizzard, enhanced meridional drift in December of 2017, and sustained reduced meridional circulation in winter of 2018.

As noted by Lukovich et al. (2021), the March 2017 blizzard within the HBC was captured by the compound extreme event of strong winds with heavy precipitation. In this section, we apply concepts from Lagrangian dispersion statistics to observational data recorded by ice drift beacons deployed off the coast of Churchill during the BaySys winter field campaign in 2017 (Figure 16, left panel). Single-particle dispersion is used to identify organized structure in the ice drift field and sea ice dynamical regimes, while three-particle dispersion is used to characterize sea ice deformation (changes in sea ice motion gradients) before, during, and following the blizzard and extreme event of March 7–9, 2017, near Churchill, Manitoba.

Ice beacon trajectories from February to March exhibit recirculation patterns and loops beyond the 50-m contour superimposed upon regional-scale cyclonic circulation (Figure 16, right panel). Specifically, beacons launched on February 4 and located near 93ºW, 59ºN on February 10 traveled northwest until the end of February and subsequently southeast until March 20 in a cyclonic circulation pattern. Superimposed on this regional scale feature are smaller-scale “loops,” in the vicinity of the symbols depicting the storm onset near 94ºW, that ensued during the storm, after which the beacons continued their regional-scale cyclonic circulation southeast.

Evolution in these trajectories is captured by single-particle dispersion (Figure 17, left panel), or the displacement of the beacons from their origin, which in this case lies at the coordinates associated with February 10 (Figure 16, right panel). In particular, total dispersion is characterized by predominantly meridional dispersion or displacements until approximately February 19, then zonal dispersion until March 11, after which meridional dispersion dominates as trajectories continue southeast. Also noteworthy are the limited total (zonal) displacements from February 22 to storm onset on March 7, and the sharp decrease in meridional displacements during the storm, characteristic of loops associated with ice-ice and ice-coast interactions resulting in displacements in the zonal direction in response to strong winds encountered during the storm. Total and meridional dispersion equilibrate following the storm, indicating limited displacement in the beacon trajectories.

Temporal scaling maps based on slopes and the transition regimes depicted in single-particle dispersion for observed ice beacon trajectories show the evolution in sea ice dynamical regimes prior to, during, and following the March 7–9, 2017, blizzard (Figure 17, right panel). Before the storm, the temporal scaling map shows scaling exponent values of $α∼1.7∼53$ and α ∼ 3 characteristic of elliptic and super-diffusive regimes until February 22, followed by a subdiffusive regime, α < 1, until March 3 and meridional (southward) advection. During the storm, sea ice dispersion is characterized by a subdiffusive regime. Following the storm, sea ice dispersion is captured by combined super- (α > 1) and subdiffusive regimes, characteristic of trapping and flight events and ice–ice and ice–coast interactions (Figure 17, right panel). In summary, sea ice dispersion is described by elliptic and super-diffusive dynamical regimes characteristic of inertial oscillations superimposed on ice–ice, ice–coast interactions, and nonlocal transport before the storm; a subdiffusive dynamical regime and “trapping” during the storm; and trapping and flight events and suppressed displacements characteristic of predominantly local interactions following the storm.

Investigation of sea ice deformation is based on triplet area and DKPs, including divergence, vorticity, shearing deformation rate, and stretching deformation rate (Figures 18 and 19). Before the storm (in early and late February), vorticity and the shearing deformation rate contribute to sea ice deformation, which we speculate can be attributed to the combined effect of inertial oscillations depicted by vorticity and the elliptic regime, and shearing due to interactions between mobile and landfast ice with the coastline. DKPs show weak deformation, evident in vanishing values during and following the March 7–9 blizzard, which may be an artifact of what is referred to as healing in Bouillon and Rampal (2015), whereby leads and cracks in the ice cover refreeze due to cold temperatures and consolidation in the ice cover. Temperatures during the blizzard decreased by approximately 10ºC. Following the storm, increased frequency in stretching rate oscillations captures elongation in the triangular configuration characteristic of filamentation in the sea ice cover, which accompanies a return to enhanced vorticity and shearing deformation rates. Relative DKPs further illustrate a decline in total ice deformation during and following the storm that is recovered after March 11. Also of interest are more subtle changes in the sea ice vorticity squared during the storm that are manifested as vanishing Okubo–Weiss values, indicating comparable contributions from total sea ice deformation and vorticity during this blizzard, preceded by predominantly shear and vorticity events and followed by alternating predominant contributions from vorticity and shear and stretching rates indicating enhanced deformation in the sea ice cover following the storm.

In summary, results from a Lagrangian dispersion analysis of ice beacons deployed in February and recording during the extreme event in March indicate distinct transitions in sea ice dynamical regimes before, during, and following the March 7–9, 2017, storm, characterized by temporal scaling maps depicting elliptic and advective, subdiffusive, and alternating sub- and super-diffusive regimes, respectively. Distinctive dynamical behavior is further reflected in DKPs and relative DKPs computed from the evolution in the triangular configuration of beacons that demonstrates sea ice deformation associated with stretching and shearing before the storm, comparable contributions during the storm, and enhanced deformation following the storm due to intermittent dominant contributions from vorticity and total deformation. This analysis provides a prescription for comparison between simulated and observed Lagrangian trajectories as the foundation for continued studies in understanding the impacts of extreme events on sea ice circulation in the HBC and as a contribution to ongoing development of an integrated observational-modeling Lagrangian framework to measure the ability of models to accurately capture sea ice dynamical features.

In this paper, we examined SSTs and sea ice conditions in the HBC as a baseline evaluation for the BaySys 2016–2018 field program time frame. The results from this study showed that SSTs were high in northwestern HB from May to July during the 2016–2018 time frame relative to the 1982–2010 climatology. Warmer SSTs were also observed throughout the annual cycle in both 2016 and 2017, with cooler SSTs observed throughout 2018. Similarly, unusually low sea ice cover existed from August to December in 2016 and from July to September in 2017, while unusually high sea ice cover characterized January, February, and October of 2018. From an evaluation of freeze-up and breakup dates during the baseline years and in comparison with the 1981–2010 climatology, we found that the ice-free season was approximately 20 days longer in 2016 than in 2018, which was representative of the climatological mean. From an assessment of ice drift speeds and the meridional circulation index (MCI), we found strong circulation with a low ice cover (high SSTs) in 2016 and 2017 and weak circulation with high ice cover (low SSTs) in 2018. In keeping with past studies (i.e., Prinsenberg 1983), we observed high drift speeds and low MCI when river discharge to the HBC was high, illustrating local interactions. Contrasting MCI anomalies were reflected in contrasting SLP anomalies, illustrating regional interactions. In particular, unusually high ice drift speeds occurred in April of 2016 and 2017 and in May of 2018, coinciding with strong winds in 2016 and 2018 and zonal atmospheric flow in 2017. Unusually strong meridional circulation was observed in spring of 2016 and in September of 2017 during low river discharge conditions, and in December of 2017 during an anomalous SLP high/low regime to the northwest/southeast of the HBC. Weak meridional circulation existed in April of 2017 following the March 2017 blizzard, indicative of ice–ice interactions, and from January to April in 2018 when the HBC experienced low SSTs and high sea ice area.

In a case study of an extreme event, the blizzard of March 7–9, 2017, evaluated using Lagrangian dispersion statistics yielded temporal scaling exponent values characteristic of inertial oscillations superimposed on ice–ice, ice–coast interactions, and nonlocal transport just prior to the blizzard; a subdiffusive regime during the storm; and combined super- and subdiffusive regimes following the storm characteristic of local and ice–ice and ice–coast interactions. The March blizzard was also shown to suppress sea ice deformation off the coast of Churchill, possibly due to refreezing in leads associated with a sudden drop in temperature. Results from this historical assessment and analysis are, in the context of a storylines approach (Shepherd et al., 2018), relevant to an investigation of possible future pathways and scenarios under continued climate change and river regulation. The Eulerian and Lagrangian diagnostics, tools, and framework developed here and in the companion paper (Lukovich et al., 2021) can be used as a foundation for a more permanent, integrated observational-modeling framework. Such a framework would allow for action on and response to relative climate change and river discharge regulation impacts on oceanographic and sea ice conditions in HB, relevant from the perspective of preparedness, adaptive management, and planning in a changing climate.

The Optimum Interpolation sea surface temperature data were downloaded from //rda.ucar.edu/datasets/ds277.7/#!access. National Snow and Ice Data Center sea ice concentrations were downloaded from https://nsidc.org/data/G02202/versions/3. National Snow and Ice Data Center sea ice drift data, Version 4, were downloaded from https://daacdata.apps.nsidc.org/pub/DATASETS/nsidc0116_icemotion_vectors_v4/north/daily/.

The supplemental files for this article can be found as follows:

Figures S1–S6. Equations. DOCX

This work is a contribution to the Natural Sciences and Engineering Council of Canada (NSERC) Collaborative Research and Development (CRD) project titled BaySys. In addition, this research contributes to the ArcticNet Networks of Centers of Excellence and the Arctic Science Partnership (ASP). The authors would also like to thank the editors Jody Deming and Stephen Ackley and two anonymous reviewers for constructive edits and suggestions.

Funding for this research was graciously provided by Manitoba Hydro, Natural Sciences and Engineering Council of Canada, Amundsen Science, and the Canada Research Chairs program.

The authors declare no competing interests.

Contributed to conception and design: JVL, SJ, AT.

Contributed to acquisition of data: SJ, JVL, DB.

Contributed to analysis and interpretation of data: JVL, SJ.

Drafted and/or revised the article: JVL, SJ, AT, PGM, JCS, KS, KW, DB, TAS, DGB.

Approved the submitted version for publication: All authors.

How to cite this article: Lukovich, JV, Jafarikhasragh, S, Tefs, A, Myers, PG, Sydor, K, Wong, K, Stroeve, JC, Stadnyk, TA, Babb, D, Barber, DG. 2021. A baseline evaluation of oceanographic and sea ice conditions in the Hudson Bay Complex during 2016–2018. Elementa: Science of Anthropocene 9(1). DOI: https://doi.org/10.1525/elementa.2020.00128

Domain Editor-in-Chief: Jody W. Deming, University of Washington, Seattle, WA, USA

Associate Editor: Stephen F. Ackley, Department of Geological Sciences, University of Texas at San Antonio, San Antonio, TX, USA

Knowledge Domain: Ocean Science

Part of an Elementa Special Feature: BaySys