On a Polynya in Makinson Inlet

• Published in: ARCTIC
• Main Author: Sadler, H. Eric
• Format: Article in Journal/Newspaper
• Language: English
• Published: The Arctic Institute of North America 1974
• Subjects: Stellaria; Hook Glacier; Makinson Inlet; Northwest Arm; St. Laurent Point; Arctic
• Online Access: https://journalhosting.ucalgary.ca/index.php/arctic/article/view/65922

A polynya was observed three kilometres south of Hook Glacier in the northwest arm of Makinson Inlet in May 1973 . it was only possible to occupy four stations in the arm: Station I near the head, Station 2 in the basin just north of Hook Island, Station 3 about 200 m east of the polynya and Station 4 east of St. Laurent Point . The results from Station 2 showed that the water was almost isothermal at -1.80 °C, near the freezing point, with little salinity variation in the vertical column. The temperature at 125 m in Station 2 was nearly 0.5 °C lower than the temperature at the same depth in Station 4 in the waters of the main section of the inlet. . The resulting estimated volume of water in the inlet is 2.4 × 10**9 m³ which is considered accurate only to within a factor of three. . The estimated cross-sectional area, 1.5 × 10**4 m² is probably accurate to a factor of 2. . The mean value adopted for the volume of the tidal prism, 1.2 × 10**8 m³, is probably accurate to a factor of 2. The rate of loss of heat through the surface of the polynya can be estimated to be about 1000 langleys per day if the air temperature is taken as -30 °C, the water temperature as -1 °C and the mean wind velocity 5 m/sec. This gives a total heat loss during each flood tide over the 2 km² of the polynya of 5 × 10**12 calories. It is assumed that more or less complete mixing of the incoming tidal flow and the waters of the arm takes place on each flood tide. This assumption is justified, as a first approximation at least, by the state of homogeneity revealed by temperature and salinity observations. The resulting degree of cooling of the water in the arm would then be 3.0 × 10**-3 °C on each flood tide. If now it is assumed that the water in the arm had a similar temperature structure to that in the main inlet at the beginning of freeze-up, the difference between the average temperature in the deep basin and that in the main inlet in May must be due to additional cooling of the inflowing water as it passes through the polynya. By integration over the upper 150 m, this mean temperature difference is found to be about 0.2 °C, and therefore under the assumed conditions about 70 tides would be required to give the observed cooling, or about 1000 degree-days. . the observed temperature distribution could be expected to occur some time in December. Until this time the polynya would remain open because of the flow on both flood and ebb tides of water above the freezing point. Once the water in the basin reached an isothermal condition with the temperature at -1.7 °C or lower, it might be expected that the very cold waters of the ebb tide would begin to freeze in the polynya. On each flood tide slightly warmer water mixed upwards from the deeper levels of the main inlet would pass through the polynya but the low temperatures of January and February and the large net heat loss due to radiation would probably be sufficient to keep the surface frozen over. With the return of the sun in April, the combination of solar heating and of ablation from below by the slightly warmer inflowing water would be expected to open the polynya sometime before the rest of the ice in the inlet broke up. When the observations were made in the middle of May the polynya was about 2 km long north to south and 1 km wide. The ice in that region of the arm even at some distance from the open water was about one third the thickness of that in the main inlet and about half the thickness of that in the basin . ERTS satellite photographs taken in 1973 show that the polynya opened some time between 4 April and 22 April, at which latter date it had a diameter of about 1 km. The ice cover around it remained continuous until July. . In summary, the water in the basin is well mixed right to the bottom, although the sill depth is less than 15 m. At the same time the polynya region appears to remain open for most of the year. The conclusion is that the two phenomena are complementary and that the homogeneity of the water is a result of the downward mixing of water cooled in its passage through the polynya. Whether the water behind the sill becomes stratified during the summer and consequently becomes partly deoxygenated at depth remains to be determined. However, it seems probable that even if this happens there is complete regeneration of the deep basin water at least every winter. .