Kate Hale, PhD

Assistant Professor | Geography Department | University of British Columbia

Waiting for the IceCube to warm up to begin sampling the specific surface area (SSA) of snowpack layers in Steamboat Springs, CO as part of CU-Boulder's Advance Snow Measurements course. Photo credit: Kehan Yang.

Becoming a snow scientist

Throughout the stages of my career, I have been involved in a number of projects across the snow science and hydrology sphere. From modeling the intricacies of catchment and continental-scale water availability to instilling snow and hydrology fundamentals in the classroom and supporting satellite missions, I strive to continually expand my skillset and impact, becoming an expert in my field. My research projects, teaching, and outreach efforts yield the opportunities to further my experience as a snow scientist, effective communicator, and environmental professional. I aim to facilitate these opportunities for my research program and community.

(a) Spatially distributed % change in annual average Budyko anomaly between the control and warming simulations. Purple shading indicates increases in partitioning of effective precipitation to runoff in the warming simulation, whereas white and tan shading indicates decreases in partitioning to runoff in the warming simulation, (b) Average PET/P and ET/P for all grid cells with a positive SSI value (purple grid cells) and 0 or negative SSI value (white and tan grid cells) in Budyko space with noted anomaly values for each simulation. The historical simulation is represented by an open circle and dashed line, and the future simulation is represented by a solid circle and solid line. The double-arrowheads represent the way in which anomaly values were calculated (y-value of black curve minus y-value of point).

Changes in snow water storage and hydrologic partitioning in an alpine catchment in the Colorado Front Range

Publication linked here: We evaluated fine-scale changes in the magnitude and duration of alpine snow water storage and release by comparing effective precipitation seasonality to that of surface water inputs using a Snow Storage Index (SSI). We forced the Distributed Hydrology Soil Vegetation Model with historical climate conditions and an end-of-century warming signal down-scaled from a 4-km regional climate model, to simulate future changes in snow water storage and partitioning of precipitation to runoff and evapotranspiration. The hydrological modeling was conducted on a 2-m spatial grid to resolve fine scale processes over a 0.6-km2 headwater catchment within the Niwot Ridge Long-Term Ecological Research site located in the Rocky Mountains, Colorado, USA. Proportionally more rainfall, reduced snowpack size and extent, and earlier snowmelt occurred in the future scenario with decreased catchment average SSI and thus snow water storing capabilities, with inordinately large decreases occurring in areas of the catchment with reconstructed snowdrifts (−57% average and −100% maximum). Using the Budyko framework to evaluate annual hydrologic partitioning, precipitation inputs to streamflow increased by a maximum 10% in large SSI regions with snowdrifts under warming conditions, signifying a potential buffer for total catchment and annual streamflow loss in a future climate (Hale et al., 2024).

Recent decreases in snow water storage in western North America

Publication linked here: Mountain snowpacks act as natural water towers, storing winter precipitation until summer months when downstream water demand is greatest. While previous studies have explored snow water equivalent trends, quantifying snowpack water storage in terms of its’ magnitude and duration has largely been ignored despite its importance to water availability for society and ecosystems. Across western North America, we introduce a Snow Storage Index (SSI), which represents the annual temporal phase difference between daily precipitation and surface water inputs – representing the sum of rainfall and snowmelt – weighted by relative volumes. Annual SSI values have decreased (p < 0.05) from 1950-2013 in over 25% of mountainous areas. The SSI decline is a result of significantly earlier snowmelt and rainfall in spring months, with additional declines in winter precipitation. Different from trends in snow water equivalent or snow fraction, the SSI represents the degree to which snow is delaying the timing and magnitude of surface water inputs relative to precipitation. The lag in timing between when precipitation falls and the delivery of that water is a fundamental component of the hydrologic cycle in snow-affected regions. The SSI offers a new perspective on changes in water delivery and related climatic sensitivities for hydrological and ecological applications (Hale et al., 2023a).

Original high-resolution figures available for download linked here.

(a) Long-term average Snow Storage Index across the mountainous western cordillera, constrained to areas within each EPA Level III ecoregion where > 0 for 1950-2013. Black points represent SNOTEL stations in the USA and CanSWE stations in Canada. Spatially distributed VIC data are shown in color, with darker blue (orange) shades indicating a greater (lower) value. The twelve EPA Level III ecoregions of the western cordillera are outlined in black and are labeled as: i) North Cascades, ii) Cascades, iii) Eastern Cascade Slopes and Foothills, iv) Klamath Mountains, v) Sierra Nevada, vi) Blue Mountains, vii) Columbia Mountains/Northern Rockies, viii) Idaho Batholith, ix) Wasatch and Uinta Mountains, x) Canadian Rockies, xi) Middle Rockies, xii) Southern Rockies. Panels (b) and (c) show exemplar grid-cell daily average precipitation (P) and surface water input (SWI) data used to calculate in the Sierra Nevada, and Southern Rockies, respectively; sine curves are shown with black lines. The vertical yellow dashed lines indicate the peak of each sine curve. The horizontal dashed arrows notate the temporal difference in the peak P and peak SWI. The vertical dotted arrows notate the amplitude of each select curve.

Annual average Snow Storage Index compared to the Budyko anomaly per grid-cell, per eco-region across the western United States. All relationships are statistically significant (linear and Spearman rank p < 0.05). Shading represents the 95% confidence interval, and Variable Infiltration Capacity grid cells are colored by average annual aridity (PET/P). Corresponding slope, linear r2 values and Spearman rank correlation values (Rs) are listed in each panel. Positive Budyko anomalies indicate overproduction of streamflow, whereas negative Budyko anomalies indicate underproduction of streamflow. Black open circles indicate the Catchment Attributes and Meteorology for Large-Sample Studies data within each eco-region.

Effects of Snow Water Storage on Hydrologic Partitioning Across the Mountainous, Western United States

Publication linked here: We employ a Snow Storage Index (SSI) to represent the annual temporal phase difference between daily precipitation and daily modeled surface water inputs (SWI, the sum of rainfall and snowmelt), weighted by the respective amounts. We coupled the SSI metric with a Budyko-based framework to determine the effect of snow water storage on relative hydrologic partitioning across snow-influenced watersheds in the western U.S. Greater snow water storage was positively correlated with greater hydrologic partitioning to streamflow, particularly in the North Cascades/Cascades (r2: 0.62), Blue Mountains (r2: 0.56), Canadian Rockies (r2: 0.55), Idaho Batholith, (r2: 0.48), and Columbia Mountains/Northern Rockies (r2: 0.45). The weekly SWI:P ratio was an equally strong predictor for hydrologic partitioning, particularly in mid-spring (e.g., March/April) in the same mountainous areas (r2: 0.62-0.74, across the same eco-regions). If SSI decreases with future warming, the volume of water partitioned streamflow will decrease non-uniformly across the western U.S. with substantial implications for ecosystems and agricultural, industrial, and domestic water supplies (Hale et al., 2023b).

Collecting depth, density, temperature, stratigraphy, ground condition, and specific surface area measurements on the North Slope of Alaska, as part of the greater NASA SnowEx campaign. Simultaneous measurements included snow layer hardness using the snow micro-penetrometer, and depth, density and snow water equivalent from ground-based radar and airborne radar, lidar, and SWESARR. Photo credit: Sveta Stuefer.

NASA SnowEx Campaign: Time Series Site Lead, Niwot Ridge, CO

SnowEx was a multi-year NASA Terrestrial Hydrology Program field experiment to address important gaps in remote sensing of snow and snowpack-derived water resources. SnowEx focused on airborne technology and ground-based field work and on comparing various sensing approaches, with an ultimate goal of globally measuring snow water equivalent from space. SnowEx thus laid a groundwork for a future snow satellite mission. My responsibilities each snow season included: measuring snow pit profiles including density, temperature, stratigraphy, liquid water content, and specific surface area (SSA); completing snow depth transects; completing ground penetrating radar (GPR) grids and terrestrial LiDAR scans (TLS); analyzing raw data for public distribution and complementary research; maintaining automated snow sensor networks at field locations. These efforts took place across the mountainous western United States, including Niwot Ridge of the Front Range, Colorado and the North Slope of Alaska.

Changes in hydrologic partitioning in the Colorado upper montane forest

Publication linked here: As the climate warms, the fraction of precipitation falling as snow is expected to decrease and the timing of snowmelt is expected to shift earlier in spring. In snow-dominated mountainous regions that rely on snowpack and snowmelt for water supply, this change in snow accumulation and melt prompts us to examine downstream changes in streamflow. The objective of this study is to understand how changes in precipitation phase and snowmelt timing alter the timing of surface water inputs (i.e. rainfall and snowmelt) and the partitioning of these inputs between evapotranspiration and streamflow. Increased streamflow generation efficiency during winter months effectively buffered the net annual streamflow decline associated with warming. This cold season buffering effect is unique to snow influenced systems, as the magnitude and timing of water released from snowpacks, and input to the surface, is sensitive to warming whereas the timing and magnitude of surface water inputs in rain-dominated systems are insensitive to warming. Seasonal streamflow buffering may diminish as warming drives many systems toward rain-dominance and may have important implications for hydrological and ecological processes and for water resource management across Earth’s snow-influenced regions (Hale et al., 2022a).

The study area for this publication was Gordon Gulch, a sub-catchment of the Boulder Creek Watershed located in the upper montane zone of the Colorado Front Range.

Drivers of spatiotemporal patterns of surface water inputs in a catchment at the rain-snow transition zone of the water-limited western United States

Publication linked here: Spatial and temporal dynamics of rainfall and snowmelt (i.e., surface water inputs, SWI) control soil moisture, groundwater recharge and streamflow at annual, seasonal, and event scales. In the rain-snow transition zone, comprising a large portion of the mountainous western United States, there is limited understanding of the sensitivity of spatiotemporal SWI dynamics across hydrologically variable water years (WYs). We modeled rainfall and snowpack dynamics in a small headwater catchment (1.8 km2) spanning the rain-snow transition in southwestern Idaho, USA, for two hydrologically distinct WYs (2011 and 2014). In wet WY 2011 and dry WY 2014, total precipitation drove spatial variability in annual SWI. Snow drifts generated more SWI (901-2080 mm) than high-elevation scour zones (442-640 mm), which generated less SWI than mid-elevation, non-drift locations (452-784 mm). Seasonally, energy fluxes differed most during the snowmelt period, where higher net radiation at lower elevations and south-facing slopes drove SWI production. At the rain-on-snow (ROS) event scale, higher elevations and north-facing slopes generated 15-20% of annual SWI, due mainly to higher turbulent fluxes. The most productive ROS events occurred after peak snow water equivalent (SWE), when rainfall fell onto ripe snowpacks. Snow drift locations were less susceptible to melt during ROS events, offset by the larger cold content and snowpack mass. Thus, catchment water resources depend on SWI magnitude, location, and timing, which are moderated by drift persistence at all temporal scales. As the climate warms, shifts in spatiotemporal SWI distribution are expected with declines in snowfall and snowfall redistribution in this area (Hale et al., 2022b).

Across Johnston Draw, located in SW Idaho and representing the semi-arid rain-snow transition zone in this work: Total annual SWI in (A) 2011, a relatively wet year (mean±sd: 692±324 mm); (B) 2014, a relatively dry year (520±175 mm), and (C) the difference in SWI between the two years (SWI 2011 – SWI 2014). (D) Boxplots show the variability in annual SWI throughout the watershed in a wet and a dry year. Median total SWI in 2011 (662 mm) was greater than median total SWI in 2014 (494 mm), as was the range and upper extent of outliers.

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