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Article Is Available On- Anderson, E Hydrol. Earth Syst. Sci., 25, 2513–2541, 2021 https://doi.org/10.5194/hess-25-2513-2021 © Author(s) 2021. This work is distributed under the Creative Commons Attribution 4.0 License. The spatial extent of hydrological and landscape changes across the mountains and prairies of Canada in the Mackenzie and Nelson River basins based on data from a warm-season time window Paul H. Whitfield1,2,3, Philip D. A. Kraaijenbrink4, Kevin R. Shook1, and John W. Pomeroy1 1Centre for Hydrology, University of Saskatchewan, Saskatoon, SK, S7N 1K2, Canada 2Department of Earth Sciences, Simon Fraser University, Burnaby, BC, Canada 3Environment and Climate Change Canada, Vancouver, BC, Canada 4Geosciences, Utrecht University, Utrecht, the Netherlands Correspondence: Paul H. Whitfield (paul.h.whitfi[email protected]) Received: 24 November 2020 – Discussion started: 4 January 2021 Revised: 30 March 2021 – Accepted: 8 April 2021 – Published: 18 May 2021 Abstract. East of the Continental Divide in the cold inte- separating the Canadian Rockies and other mountain ranges rior of Western Canada, the Mackenzie and Nelson River in the west from the poorly defined drainage basins in the basins have some of the world’s most extreme and variable east and north. Three specific areas of change were iden- climates, and the warming climate is changing the landscape, tified: (i) in the mountains and cold taiga-covered subarc- vegetation, cryosphere, and hydrology. Available data consist tic, streamflow and greenness were increasing while wetness of streamflow records from a large number (395) of natu- and snowcover were decreasing, (ii) in the forested Boreal ral (unmanaged) gauged basins, where flow may be peren- Plains, particularly in the mountainous west, streamflows nial or temporary, collected either year-round or during only and greenness were decreasing but wetness and snowcover the warm season, for a different series of years between were not changing, and (iii) in the semi-arid to sub-humid 1910 and 2012. An annual warm-season time window where agricultural Prairies, three patterns of increasing streamflow observations were available across all stations was used to and an increase in the wetness index were observed. The classify (1) streamflow regime and (2) seasonal trend pat- largest changes in streamflow occurred in the eastern Cana- terns. Streamflow trends were compared to changes in satel- dian Prairies. lite Normalized Difference Indices. Clustering using dynamic time warping, which overcomes differences in streamflow timing due to latitude or elevation, 1 Introduction identified 12 regime types. Streamflow regime types exhibit a strong connection to location; there is a strong distinction Western Canada, east of the Continental Divide, has extreme between mountains and plains and associated with ecozones. and variable climates and is experiencing rapid environmen- Clustering of seasonal trends resulted in six trend patterns tal change (DeBeer et al., 2016) where a changing climate that also follow a distinct spatial organization. The trend is affecting the landscape, the vegetation, and the water. The patterns include one with decreasing streamflow, four with southern part of this region sustains 80 % of Canada’s agri- different patterns of increasing streamflow, and one with- cultural production, a large portion of its forest wood, and out structure. The spatial patterns of trends in mean, min- pulp and paper production and also includes several glob- imum, and maximum of Normalized Difference Indices of ally important natural resources (e.g. uranium, potash, coal, water and snow (NDWI and NDSI) were similar to each other petroleum). Understanding both observed changes and possi- but different from Normalized Difference Index of vegeta- ble future changes is clearly in the national interest. Climate tion (NDVI) trends. Regime types, trend patterns, and satel- variation and change have been demonstrated to have impor- lite indices trends each showed spatially coherent patterns tant effects on the rivers of Canada (Whitfield and Cannon, Published by Copernicus Publications on behalf of the European Geosciences Union. 2514 P. H. Whitfield et al.: The spatial extent of hydrological and landscape changes 2000; Zhang et al., 2001; Whitfield et al., 2002; Janowicz, Streamflow data in this domain are taken from stations 2008; Déry et al., 2009a, b; Tan and Gan, 2015), includ- that were operated either year-round or seasonally (MacCul- ing Western Canada’s cold interior (Luckman, 1990; Burn, loch and Whitfield, 2012); seasonal stations generally pro- 1994; Luckman and Kavanaugh, 2000; Ireson et al., 2015; vide records from April through the end of October, be- Dumanski et al., 2015; Ehsanzadeh et al., 2016). The sensi- cause there is either no streamflow in the winter or because tivity of streamflow to changes in temperature and precip- the channels become completely frozen. This approach con- itation may differ by period of the year (Leith and Whit- trasts with many studies that use only stations having contin- field, 1998; Whitfield and Cannon, 2000; Botter et al., 2013). uous records and a common period of years (e.g. Whitfield Trends in water storage, based on Gravity Recovery and Cli- and Cannon, 2000); one novel aspect of this study is that it mate Experiment (GRACE) satellites, identified precipitation demonstrates a method which incorporates records from both increases in northern Canada, a progression from a dry to a continuous and seasonal stations. Trend assessment is con- wet period in the eastern Prairies/Great Plains, and an area ducted on an annual common time window for both continu- of surface water drying in the eastern boreal forest (Rodell ous and temporary streams. et al., 2018). The Mackenzie and Nelson (Saskatchewan Landscape changes may cause or result from hydrological and Assiniboine–Red) River basins were the focus of this changes. Satellite imagery and derived spectral indices were study and are where cold-region climatic, hydrological, eco- used to assess the changes in the landscapes of basins in re- logical, and cryospheric processes are highly susceptible to lation to their hydrological response. Normalized Difference the effects of warming. Both rivers arise in the Canadian Indices of vegetation, water, and snow (NDVI, NDWI, and Rockies and receive the vast majority of their runoff from NDSI) were constructed using optical imagery from the The- high-elevation headwater basins that are dominated by heavy matic Mapper (TM) sensor (USGS and NOAA, 1984) on- snowfall, long-lasting seasonal snowcover, glaciers, and ice- board the Landsat 5 satellite for individual basins (e.g. Hall fields. The whole region is subject to strong seasonality, con- et al., 1995; Su, 2000; Hansen et al., 2013; Pekel et al., 2016). tinental climate, near absence of winter rainfall, and season- The temporal coverage of the indices differs from that of the ally frozen soils. From the mid-boreal forest northwards and hydrometric data used in this study. Trends in these indices at high elevations, the surface is an annually thawed active over many basins from the satellite imagery that is avail- layer below which materials are permanently frozen (per- able provides a complementary perspective on hydrological mafrost). Tens of millions of lakes and wetlands cover the change over the study domain. northern and eastern parts of this region, where the Cana- The objective of this study was to examine the hydrologi- dian Shield dominates topography and hydrography. Cold cal structure and changes in seasonal streamflow patterns by winters and coincidence of the precipitation maximum with combining data from perennial and temporary streams to di- the snowmelt period or postmelt period mean that rivers and agnose hydrological process differences and change across streams have minimum flows in late winter and maximum Western Canada’s cold interior. Linking continuous and sea- flows in late spring. This study provides a statistical assess- sonal data from a large number of hydrometric stations using ment of patterns and recent changes in the warm-season hy- only warm-season data, three important questions were ad- drological regime and in satellite indices of vegetation, water dressed in this study domain. storage, and snow and of the spatial patterns of these changes 1. How are the hydrological types and processes dis- at gauged basins across this large domain. tributed? Hydrological processes differ widely in this domain, which spans 11 of Canada’s 15 terrestrial ecozones and in- 2. How are climate-related trends distributed? cludes many small basins where streamflow is only tempo- 3. Are some hydrological types and processes more sus- rary (Buttle et al., 2012). The hydrographs of all rivers in this ceptible to change over time? domain reflect contributions from snowmelt, the magnitudes of which differ in both space and time. Other flow contribu- By examining trends in normalized difference indices for tions, from glaciers and rainfall, all vary spatially across the basins, this study also addresses whether there are changes domain, with glacier contributions focussed in high mountain that may be driving or following the hydrological change be- headwaters and rainfall contributions increasing at lower ele- ing observed. vations and latitudes. Ecozones (Marshall et al., 1999; Eamer et al., 2014; Ireson et al., 2015) were chosen as an appropri- 2 Methods ate level for comparisons rather than physical attributes such as climate, permafrost, or geology, since ecozones represent 2.1 Data regions where
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