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The contribution of cold-season soil respiration to the Arctic-boreal carbon cycle and its potential feedback to the global climate remain poorly quantified, partly due to a poor understanding of changes in the soil thermal regime and liquid water content during the soil-freezing process. Here, we characterized the processes controlling active-layer freezing in Arctic Alaska using an integrated approach combining in situ soil measurements, local-scale (similar to 50 m) long-wave radar retrievals from NASA airborne P-band polarimetric SAR (PolSAR) and a remote-sensing-driven permafrost model. To better capture landscape variability in snow cover and its influence on the soil thermal regime, we downscaled global coarse-resolution (similar to 0.5 degrees) MERRA-2 reanalysis snow depth data using finer-scale (500 m) MODIS snow cover extent (SCE) observations. The downscaled 1 km snow depth data were used as key inputs to the permafrost model, capturing finer-scale variability associated with local topography and with favorable accuracy relative to the SNOTEL site measurements in Arctic Alaska (mean RMSE = 0.16 m, bias = 0.01 m). In situ tundra soil dielectric constant (epsilon) profile measurements were used for model parameterization of the soil organic layer and unfrozen-water content curve. The resulting model-simulated mean zero-curtain period was generally consistent with in situ observations spanning a 2 degrees latitudinal transect along the Alaska North Slope (R: 0.6 +/- 0.2; RMSE: 19 +/- 6 days), with an estimated mean zero-curtain period ranging from 61 +/- 11 to 73 +/- 15 days at 0.25 to 0.45m depths. Along the same transect, both the observed and model-simulated zero-curtain periods were positively correlated (R > 0.55, p < 0.01) with a MODIS-derived snow cover fraction (SCF) from September to October. We also examined the airborne P-band radar-retrieved epsilon profile along this transect in 2014 and 2015, which is sensitive to near-surface soil liquid water content and freezethaw status. The epsilon difference in radar retrievals for the surface (similar to<0.1 m) soil between late August and early October was negatively correlated with SCF in September (R = 0.77, p < 0.01); areas with lower SCF generally showed larger epsilon reductions, indicating earlier surface soil freezing. On regional scales, the simulated zero curtain in the upper (< 0.4 m) soils showed large variability and was closely associated with variations in early cold-season snow cover. Areas with earlier snow onset generally showed a longer zero-curtain period; however, the soil freeze onset and zero-curtain period in deeper (> 0.5 m) soils were more closely linked to maximum thaw depth. Our findings indicate that a deepening active layer associated with climate warming will lead to persistent unfrozen conditions in deeper soils, promoting greater cold-season soil carbon loss.