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2.2: Soils of the Prairie Provinces

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    Dan Pennock

    Learning Objectives

    Upon completion of this chapter, students will be able to:

    1. Describe the factors responsible for the distribution of soils in the Prairie Provinces
    2. Identify the diagnostic soil horizons associated with soil orders and great groups (according to the Canadian System of Soil Classification) of the Prairie Provinces
    3. Relate the major land uses of the region with the properties of the soils


    The soils of the three Prairie Provinces have experienced the greatest conversion to agricultural land uses of any region of Canada. In most of the southern portion of this region more than 80% of the land is agricultural (Prairie Farm Rehabilitation Administration, 2000). Throughout this region the specific type of agriculture is closely linked to the capability of the soil, and hence the pattern of agricultural land use is largely determined by the pattern of the soils themselves. Although we typically refer to Alberta, Saskatchewan and Manitoba as the Prairie Provinces, it is important recognize that the true prairies generally occupy only the southern portion of these provinces.


    The regional pattern of soil distribution (Figure 10.1) is determined by the bedrock geology and the effect of the Western Cordillera on the regional climate. These two factors largely determine the patterns of soil and vegetation in the region.

    Figure 10.1. Map of soil great groups (according to the Canadian System of Soil Classification) for the Prairie Provinces. Map is a reproduction of an official work published by the Government of Canada and is based on the 1:1,000,000 Soil Landscapes of Canada map. Map courtesy of Darrel Cerkowniak, Agriculture and Agri-Food Canada. © Darrel Cerkowniak, Agriculture and Agri-Food Canada, is licensed under a CC BY (Attribution) license.

    The Prairie Provinces are underlain by approximately ⅓ igneous and metamorphic rocks of the Canadian Shield and ⅔ sedimentary rocks (Figure 10.2). The Canadian Shield underlies the eastern and north-eastern portion of the region, and sedimentary rocks the remainder. As discussed in Chapters 2 and 8, the glacial sediments that form the parent materials of soils closely reflect the nature of the bedrock that underlies them; igneous rocks yield acidic, sandy and gravelly parent materials and sedimentary rocks produce neutral, alkaline, loamy parent materials. The parent materials produced by sedimentary rocks are a mixture of gravel and sand, silt, and clay.

    Figure 10.2. Map of bedrock geology of the Prairie Provinces. The rocks of the Canadian Shield are igneous and metamorphic. The sedimentary rocks are arranged from the oldest (Ordovician) to youngest (Tertiary). Reproduced from Michalyna et al. (1978) and licensed under the Open Government Licence – Canada.

    Research on tills in this region has shown that rock fragments greater than 1 mm in diameter are derived from the Precambrian rocks of the Canadian Shield to the NE of the sedimentary rock area, whereas the sand, silt, and clay fractions normally reflect nearby geological formations (St. Arnaud, 1976). The glacial tills also contain carbonates and soluble magnesium and sodium salts. The carbonate content of the tills is highest (>40% calcium carbonate equivalent) in the Interlake area of Manitoba where surface exposure of Paleozoic limestones occurs. The carbonate content of tills decreases across the region to about 6 to 10% in much of southern Alberta and 1 to 6% in central Alberta (St. Arnaud, 1976). The carbonate content rises to 10 to 16% in the Cordilleran regions of Alberta in the region of deposition of glacial sediments from the Cordillera itself.

    The northern boundary of the continuous Chernozemic region is found north of Edmonton in Alberta and then trends to the south-east until it ends just north of Winnipeg (Figure 10.1). This NW-SE trending boundary reflects in part the influence of the Western Cordillera on the passage of moist, temperate air masses from coastal British Columbia into the western interior (discussed in Pennock et al., 2011). The air masses are deflected to the north by the high mountain ranges of southern Alberta and pass through the Cordillera via the lower elevations of the Peace River area of British Columbia and Alberta around Grand Prairie. The air masses then trend to the SE through the rest of the Prairie region. The more temperate climates of the Peace River region, which occur because of this movement of air masses, allow extensive agricultural development throughout the region and even the development of a pocket of Chernozemic soils around Grand Prairie (Figure 10.1).


    At the broadest scale, the sedimentary rock region has multiple zones of soils that radiate out from SW Saskatchewan and SE Alberta (Figure 10.1). The dominant soil order in the southern part of this region is the Chernozemic order, which formed in the grasslands that were found in this area prior to European settlement. Throughout most of the region, the Chernozemic soils are bounded by soils of the Luvisolic order, which are associated with the mixed deciduous-coniferous forest characteristic of the northern part of this region.

    Brunisolic soils are the dominant soil order on the Canadian Shield and consists of acidic forest soils develop on the sand and gravelly parent materials characteristic of this area. In north-central Manitoba a large area of glacio-lacustrine silts and clays were deposited (Figure 10.3) and Luvisolic soils have formed in these parent materials.

    Closer to Hudson Bay, the rebound of the land surface after glaciation has created a poorly drained region of near-level beach ridges and former shorelines with saturated soils. The cold temperatures and permanent water saturation has led to the development of thick layers of peat and formation of permanently frozen layers within the peats. These soils are classified as Organic Cryosols in the CSSC (Figure 10.1).

    Figure 10.3. Major soil parent materials found in the Prairie Provinces. Map is a reproduction of an official work published by the Government of Canada and is based on the 1:1,000,000 Soil Landscapes of Canada map. © Darrel Cerkowniak, Agriculture and Agri-Food Canada, is licensed under a CC BY (Attribution) license.

    The complex pattern of soils in northern and north-eastern Alberta (Figure 10.1) departs from the overall zonation of soils. In this area there are several major uplands (such as the Caribou Mountains) that are elevated plateaus occupied by Gray Luvisols and Organic Cryosols. The uplands are separated by wide valleys occupied by the Athabasca, Hay and Peace Rivers. The relatively level valleys have a complex mixture of sandy Brunisolic, loamy Luvisolic and Fibrisol Organic soils. The extensive area of oil sand extraction near Fort McMurray devastates these soil landscapes, and reclamation of the landscapes (and remediation of the spoil from oil sands operations) is a major activity for soil scientists in this region.

    Finally, the Cordilleran region at the Alberta-British Columbia border has a complex mixture of forested soils and exposed rock faces. The regional map (Figure 10.1) shows areas of exposed rock and both Dystric and Eutric Brunisolic soils, but areas of Gray Luvisolic soils also are found as well as Cryosolic alpine tundra soils at higher elevations.


    The zonal pattern of great groups of the Chernozemic order reflects the different types of grasslands that once occupied the area (and the regional climates responsible for the zonation of grasses) (Fuller, 2010; Pennock et al., 2011). These grasses were responsible for organic carbon inputs into the soil, and the colour of the diagnostic Ah horizons reflects differences in the amount of organic carbon additions from the various grass communities. The great groups of the Chernozemic order are based on the colour differences of the A horizons.

    The major climate attribute that varies across the region is the mean annual water deficit (Pennock et al., 2011, Table 10.2). The driest portions of the region have annual water deficits of approximately 200 mm and the native grasses of this region were low grasses with limited above- and below-ground biomass. The lower organic carbon inputs lead to the development of soils of the Brown Chernozemic great group (Figure 10.4). The water deficit decreases west and north of this dry region, and greater organic carbon inputs lead to formation of Dark Brown Chernozemic soils and Black Chernozemic soils. The highest organic carbon levels occur in southern Manitoba where the annual water deficit is only approximately 70 mm.

    Figure 10.4. Examples of major soils of the Chernozemic and Luvisolic great groups found in the Prairie Provinces. Soils of the Chernozemic order have organically enriched A horizons (Ah) overlying decalcified and slightly reddened Bm horizons. The upper C horizon has concentrated secondary calcium carbonate (Cca) overlying largely unaltered parent material (Ck) with lower calcium carbonate contents. The Dark Gray Chernozem is transitional to the Gray Luvisolic soils and has an A horizon with both organic accumulation and bleaching (Ahe horizon). The forested Gray Luvisols have a leaf litter layer (LFH) on top of the mineral soil horizons. The uppermost bleached Ae horizon overlies a B horizon with higher clay levels than the Ae (Bt horizon). © “Brown, Dark Brown, Dark Gray Chernozem: Saskatchewan Center of Soil Research; Black Chernozem: Roly St. Arnaud (Saskatchewan Center of Soil Research); Dark Gray Luvisol: Kent Watson (Saskatchewan Center of Soil Research)” is licensed under a CC BY (Attribution) license.

    Within these broad soil zones there are many pockets of other soil classes in the former grassland areas (Figure 10.1). During melting of the ice sheets glacio-lacustrine silts and clays were deposited in vast glacial lakes throughout the region, with large areas of deposition in west-central Saskatchewan, southern Manitoba, and north-central Manitoba (Figure 10.3). In the former, grassland region the high-clay soils of the Vertisolic order form in these glacio-lacustrine deposits (Anderson, 2010a; Brierly et al., 2011). The great groups of the Vertisolic order (Figure 10.5) reflect the differences in organic carbon inputs discussed for the Chernozems above: Vertisols in southern Saskatchewan are classified into the Vertisol great group, whereas the higher organic inputs that occur in the region south of Winnipeg result in Humic Vertisols (Figure 10.1).

    Figure 10.5. Great groups of the Vertisolic order. Mixing of soil by shrinking and swelling of clays prevents visually distinct horizons from forming. The mixed horizons are assigned a ‘v’ suffix, and in lower horizons polished surfaces (slickensides, assigned a ‘ss’ suffix) form on the face of fractures in the soil. The Humic great groups have higher organic matter inputs and a more distinct Ah horizon that the Vertisol great group. © “Vertisol: Roly St. Arnaud (Saskatchewan Center of Soil Research); Humic Vertsol: Darwin Anderson (Saskatchewan Center of Soil Research)” is licensed under a CC BY (Attribution) license.

    The distribution of Solonetzic soils is largely controlled by the presence of sodium-rich bedrock within a few meters of the soil surface rather than a particular type of glacial sediment (Anderson, 2010b; Miller and Brierley, 2011). In both Alberta and Saskatchewan, the marine shales of the Cretaceous-aged Bearpaw formation are the main bedrock type associated with Solonetzic soils. Movement of soil water and groundwater circulates sodium through the soil profile, which can lead to vertical movement of clay from the surficial Ah horizon soil to the B horizon and formation of a bleached, eluvial Ae horizon overlying the B horizon. The B overlies a saline and carbonate-rich C horizon (Csk).

    The great groups of the Solonetzic order reflect the degree of development of the Ae horizon and the AB horizon, which forms through weathering of the upper B horizon. In the Alkaline Solonetz great group the Ae is very thin or absent, and the B horizon is high in sodium (Bn) but often without higher clay levels than the Ah (Figure 10.6). The Solodized Solonetz great group has an Ae greater or equal to 2 cm thick and an intact Bnt or Bn horizon with well-developed columnar structure. In the Solod great group the top of the Bnt has disintegrated through weathering and this weathered layer forms a transitional AB horizon between the Ae and the Bnt horizons. The Solodized Solonetz great group is the most common in the landscape (Figure 10.1).

    Figure 10.6. Great groups of the Solonetzic order. The great groups of the Solonetzic order reflect the progressive disintegration of the upper part of the Bnt horizon (a horizon enriched in both sodium and clay) to form a transitional AB horizon. The AB horizon begins to form in the Solodized Solonetz great group and reaches maximum thickness in the Solod great group. © “Solonetz: Darwin Anderson (Saskatchewan Center of Soil Research); Solodized Solonetz: Roly St. Arnaud (Saskatchewan Center of Soil Research); Solod: Saskatchewan Center of Soil Research” is licensed under a CC BY (Attribution) license.

    Small areas dominated by Regosolic soils (VandenBygaart, 2011) are also found throughout the region. Regosolic soils are associated with unstable land surfaces (such as river floodplain or sand dunes) where soil development is limited to development of an Ah horizon either directly overlying the C horizon or with a thin (<5 cm) Bm between the A and C horizons (Figure 10.7). The Regosol-dominated areas in the Prairie Provinces are associated with sandy fluvial or glaciofluvial deposits along river valleys or areas of active or recently stabilized sand dunes such as the Great Sand Hills of Saskatchewan. As well, the knolls in many cultivated landscapes in the Prairie Provinces have experienced considerable soil loss due to tillage erosion, and thin Ap (p for ploughed) horizons directly overlay Cca horizons on these hill crests.

    Figure 10.7. Regosolic soils. Regosolic soils occur in very young sediments (such as on active floodplains or in active sand dune areas) or due to erosion of surface soils in cultivated fields. In all cases, B horizon formation is either absent or less than 5 cm thick. © “River sediments: Darwin Anderson (Saskatchewan Center of Soil Research); Truncated soil: Dan Pennock (Saskatchewan Center of Soil Research); Dune Sand: Roly St. Arnaud (Saskatchewan Center of Soil Research)” is licensed under a CC BY (Attribution) license.

    Many of the glacial landforms in the area are associated with melting in-place of stagnant ice masses, and the resulting land surface is a very complex assemblage of small knolls and depressions. This land surface is labelled as hummocky or knob and kettle on soil maps. Wetlands on these surfaces are often occupied by Gleysolic soils, whose Bg and Cg horizons have dull gray colours and, in some cases, patches of reddish oxidized iron within the dominantly gray material (Figure 10.8) (Bedard-Haughn, 2010, 2011). Texture-contrast horizons are also common in these soils, with a Btg horizons underlying a mottled Aeg horizon. Soils with a Btg horizon are classified into the Luvic Gleysol great group.

    Figure 10.8. Gleysolic soils. The Luvic Gleysol great group soil developed in clay loam till has dull, grayish colours throughout and small reddish mottles in the Aeg horizon. The Gleysol great groups soil developed in sandy glaciofluvial parent materials has much brighter coloured mottles throughout with maximum expression of oxidized iron in the Bg3 horizon. © Both slides: Darwin Anderson (Saskatchewan Center of Soil Research) is licensed under a CC BY (Attribution) license.

    A final soil class that is largely unmapped are saline soils. As discussed in Chapter 8, the Canadian System of Soil Classification (CSSC) does a poor job of identifying saline soils. This is in part due to the very dynamic nature of soil salinity, which fluctuates considerably due changes to soil water and groundwater flow patterns. Salinity can only be recognized in profile descriptions through the use of the suffixes s and sa in horizon labels (e.g., Csa, Cs, Bsa, Ahsa, etc.). Agriculture and Agri-Food Canada has mapped soil salinization risk for several decades as part of its Agri-Environmental Indicators program and the main areas that are vulnerable to salinization (i.e., areas mapped as moderate, high, and very high risk) are widespread throughout the Prairie region. The largest areas are the region stretching NE from Calgary to almost Saskatoon, SW Alberta, in SE Saskatchewan near Estevan, and in areas of Manitoba south of Brandon and of Winnipeg. The AAFC maps show that the risk of salinization has decreased since the 1980s due to adoption of no-till cultivation practices and the near-elimination of tillage summer fallow throughout this region.


    At the northern boundary of the Chernozemic soils the grasslands become increasingly interspersed with clumps of trees and shrubs and ultimately the forest forms an almost continuous cover over the soil. The transitional grassland-forest zone is referred to as the Parkland zone, and the continuous forest cover as the Mixedwood forest, reflecting the forest cover of deciduous and coniferous species.

    In the Parkland, the inputs of organic carbon from grasses decrease and leaf litter from trees builds up on the soil surface as a LFH layer. The colour of the Ah horizon grows lighter, and bleaching of the horizon also begins to occur, forming a surface A horizon with both humus inputs (given an ‘h’ suffix) and bleaching (an ‘e’ suffix) – the Ahe horizon. These soils are classified into the Dark Gray Chernozemic great group.

    North of the forest-grassland transition zone, organic inputs form a discrete layer laying on top of the mineral soil (the LFH layer) and the soils have a well-developed bleached layer (Ae horizon) overlying a B horizon with higher clay levels (Bt horizon). The Bt horizon is underlain by a C horizon with secondary (Cca) or primary (Ck) carbonates. These soils are classified into the Gray Luvisolic great group (Figure 10.9), which dominates the forested landscapes underlain by neutral-alkaline tills (Pettapiece et al., 2010; Lavkulich and Arocena, 2011). Gray Luvisols also occur in the large area of glacio-lacustrine parent materials in north-central Manitoba.

    Figure 10.9. Luvisolic and Brunisolic soils. Soils of the Gray Luvisol great group have well developed texture contrast (Ae and Bt) horizons overlying the C horizons with primary (Ck) and secondary (Cca) calcium carbonate. Both of the great groups of the Brunisolic order develop primarily in sandy parent materials and have the diagnostic Bm horizon. The great groups differ on the acidity of the parent materials: Dystric Brunisols develop in acidic parent materials, and Eutric Brunsiols develop in neutral pH parent materials. © “Luvisol: Darwin Anderson (Saskatchewan Center of Soil Research); D. Brunisol and Eut. Brunisol: Saskatchewan Center of Soil Research” is licensed under a CC BY (Attribution) license.

    At the boundary between the sedimentary rocks of the Interior Plains and the Canadian Shield a complex assemblage of forest and wetland soils occurs (Figure 10.1). The forested soils form in parent materials that include sandy sediments from the Canadian Shield and pulverized sedimentary rocks, which raises the pH of the parent materials above 5.5. These soils are classified into the Eutric Brunisol great group (Figure 10.9) (Smith et al., 2011). In low lying areas, water collects and forms large fens and bogs. In these wetlands peat builds up due to the permanent water saturation and soils of the Mesisol great group of the Organic order occur (Bedard-Haughn, 2010). These soils have intermediate levels of decomposition of organic materials (Figure 10.10).

    Figure 10.10. Organic and Cryosolic soils. Both soils have a thick buildup of peat in either largely undecomposed (Of) or moderately decomposed (Om) layers. The Organic Cryosol has permafrost within 1 m of the surface (note – total length of white tape is 1.2 m). © “Mesisol: Ken Van Rees (Saskatchewan Center of Soil Research); Cryosol: Saskatchewan Center of Soil Research” is licensed under a CC BY (Attribution) license.

    The dominant soil of the Canadian Shield itself are Dystric Brunisols (Figure 10.9) that develop in the acidic (pH < 5.5) sand and gravel parent materials characteristic of this region. Like the Eutric Brunisols, the Dystric Brunisols soils are very sandy soils and soil formation is limited to reddening of the B horizon and, in some cases, formation of a bleached Ae horizon. In moister forested regions of Canada, these conditions lead to formation of soils of the Podzolic order (Sanborn et al., 2011). There are also significant areas where exposed rock is the dominant surface with only scattered pockets of soils interspersed in the landscape (Figure 10.1).

    Finally, the near-level landscapes of the Hudson Plains ecozone are mainly occupied by organic soils that have a layer of permafrost (i.e., permanently frozen soil) within the soil profile. These soils have thick organic layers but, because of the permafrost, are classified into the Cryosolic order (Figure 10.10) (Tarnocai and Bockheim, 2010).


    Soil properties have a major impact on agricultural capability throughout the Prairie Provinces. The agricultural capability of soils throughout southern Canada was evaluated by the Canada Land Inventory (CLI) (see Chapter 8). The criteria used in the CLI system were based on soil and climate and remain generally applicable although cropping systems used in the region have changed greatly since the period of the CLI inventory (roughly 1965-1975). At that time the dominant crop was spring wheat and summerfallow (i.e., a year of fallow with tillage of the soil to suppress weed growth following a year of wheat) was the dominant tillage practice. Currently, a much wider range of crops (e.g., canola, pulse crops, flax) is grown, and the great majority of producers practice continuous cultivation with high amounts of crop residue left on the soil surface (i.e., conservation tillage or no-till).

    In the CLI rankings, classes 1 through 4 are considered to be capable of sustained use for cultivated field crops. In class 1 land, there are no significant constraints to crop growth, whereas in class 3 and 4 areas the range of crops is restricted and special management measures are needed to conserve the soil. Classes 5 and 6 are only suitable for forage production and are most commonly used for grazing of livestock.

    The major soil property that determines agricultural capability in the CLI system is soil texture due primarily to its effect on water availability. Secondary properties of relevance are unfavorable soil structure associated with Solonetzic soils and the presence of salinity in the soil profile. Soils that have experienced erosion of the organic-rich A horizons through time are also downgraded – organic matter has many beneficial properties including a high water-holding capacity and high nutrient-supplying power.

    All agricultural regions of the Prairie Provinces experience a water deficit (as discussed above) and hence the ability of the soil to hold water during dry periods is critical. This property is termed the available water capacity (see Chapter 4). Generally, fine-textured soils (clay, heavy clay, silty clay, clay loam) retain the highest amounts of water even in drought conditions and have high available water capacity. Medium-textured soils (silty clay loam, sandy clay loam, loam, silt loam, fine and very fine sandy loam) have lower ability to hold water during droughts but have slightly higher available water capacity. Medium-coarse sandy loam, loamy sand, and sand soils have both very low ability to hold water during droughts and low available water holding capacities and hence are the lowest rated for agriculture.

    The second major factor that determines the CLI class is the climate. In the Prairie Provinces, both moisture and heat can be limiting. Agriculture and Agri-Food Canada developed agro-climatic regions throughout Canada based on three climate factors: Mean annual precipitation, average number of frost-free days, and degree days above 5.5°C (Table 10.1 and Figure 10.11). The latter is a cumulative measure of the period when the temperature is high enough for significant plant growth. The class limits will have shifted somewhat due to climate change but the general pattern would be unchanged.

    Figure 10.11. Agro-climatic regions of the agricultural areas of the Prairie Provinces. Reproduced from Michalyna et al. (1978) and licensed under the Open Government Licence – Canada.

    Soil texture is directly inherited from the parent materials in the Prairie Provinces; hence, a clear link between agricultural capability and the soil classes described above. At the driest end of the spectrum are the Regosolic soils formed in sandy glacio-fluvial sediments or sand dune areas, which typically have CLI classes of 5 or 6. At the other end of the spectrum are Vertisol soils, which inherently have clay or heavy clay textures and typically have CLI class 1 or 2 ratings throughout the main agricultural region.

    The capability ratings for Chernozemic soils depends primarily on texture and on climate zone. The general pattern is clear from Figure 10.12: fine-textured soils are the best agricultural soils in each climate region and coarse textured soils the worst. The range is greatest for medium-textured soils developed on glacial till, which are the most common in the region.

    Figure 10.12. Matrix of Canada Land Inventory (CLI) classes associated with soil zones, soil textures, and agro-climatic zones in the Prairie Provinces. © Dan Pennock, Univ. of Saskatchewan is licensed under a CC BY (Attribution) license.

    Gray Luvisolic soils have a number of limitations for annual crop production (Pettapiece et al., 2010). The Gray Luvisols occur in zones 2H and 3H (Figure 10.11) where lack of heat and frequent frosts limit growth. The Gray Luvisols lack an Ah horizon and typically have silty textured surface mineral horizons; both factors contribute to problems with seedbed preparation and crop growth generally. Compared to Chernozemic and Vertisols soils they are also deficient in nitrogen, phosphorus, and sulphur. The Gray Luvisols and related soils in the Aspen Parkland region are widely used for forage crop production and grazing – about two-thirds of western Canada’s cattle and more than 80% of the forage crops are produced in this region (Thorpe and Anderson, 2010).

    Secondary soil properties that strongly affect agricultural capability are factors such as the presence of high sodium soils or salinity, both of which are generally associated with class 5 or 6 soils. The Bn or Bnt horizon associated with the Solonetzic soils are difficult for plant roots to penetrate and hence only the horizons above these horizons can be fully exploited by roots for nutrients and water. As well, the Ah and Ae horizons above the dense B horizons have often experienced erosion, and the variable depth of surface soil over the B horizon often gives crops on Solonetzic surfaces a wavy appearance due to lower growth on thin soils and higher growth on thicker soils. Salinity has a severe effect on crop growth and on highly saline soils growth of any plant except saline-tolerant species is impossible.

    An important landscape factor that affects the rating of medium-textured soils is topography – generally the rougher the topography, the lower the rating. Many medium-textured glacial till landscapes have many knolls and wetlands associated with them, and these cause difficulties in farm operations and uneven plant growth. Rough topography generally causes a given area to drop by at least one class in the CLI rating.

    Table 10.1. Agro-climatic regions. (Adapted from Michalyna et al. 1978)

    Mean annual
    precipitation (cm)
    Average frost-free
    period (days)
    above 5.5oC
    1 40-45 >90 1225-1670 Climate is suitable to permit growing of all dryland crops that are typical to the prairie region
    2A 30-40 >90 1330-1670 Precipitation limits growth in approximately 50% of years
    3A 27-35 90-120 1330-1670 Precipitation is a severely limiting factor for crop growth
    2H 40-50 75-90 1060-1225 Precipitation is adequate but some frost damage to crops in approximately 30% of years
    3H 27-35 <75 1000-1112 Precipitation adequate by high incidence of frost damage to crops
    5H 27-35 <60 <950 Average frost-free period too short for annual crop production

    Soil properties also play an important role in determining land capability for forest harvest operations. Forest harvest has increased in Alberta since early 2000s (from 82 thousand hectares (t ha-1) in 2005 to 92 t ha-1 in 2016). However, it has declined in Saskatchewan (42 t ha-1 in 2005 to 22 t ha-1 in 2016) and Manitoba (14 t ha-1 in 2005 to 8 t ha-1 in 2016) (all statistics from Natural Resources Canada). In total, this represents about 13% (2005) to 15% (2016) of total forest area harvested in Canada.

    The Canada Land Inventory also rated soils for forest capability in the portion of the forest where commercial forestry existed. The highest class of land in the Prairie Provinces was only class 3 due to climate constraints for tree growth throughout the region. Generally, forests on Gray Luvisol soils are rated as class 4 (Alberta and Manitoba) or Class 5 (Saskatchewan) with small areas rated one class higher in all provinces. Forests on both Eutric and Dystric Brunisolic soils are generally rated as class 6 due to significant growth constraints. Detailed ecosite guides have been prepared for each province (see Suggestions for Further Reading) that rate soils on soil texture and soil drainage – generally well-drained, fine- and medium-textured soils are the most highly rated in the forest landscape.

    Wetland soils in the Prairie Provinces are key contributors to two transnational and global issues: the protection of waterfowl in North America and the removal of carbon from the atmosphere by increasing soil organic carbon levels (carbon sequestration). In the former grassland areas of the Prairies, the complex hummocky land surfaces have countless wetlands that are occupied by Gleysolic soils or, in some cases, saline soils. These wetlands are the seasonal home for vast numbers of migratory waterfowl, and protection of Prairie wetlands is essential for preservation of waterfowl habitat. The North American Waterfowl Management Plan (NAWMP) is a major agreement among Mexico, the USA and Canada and protection of Prairie wetlands is a key aspect of this transnational plan.

    Gleysolic wetlands and especially Organic soils are repositories for large amounts of carbon. Drainage of these wetlands for agriculture causes mineralization of this carbon and its release (as carbon dioxide) to the atmosphere. The restoration of wetlands and of the wetland vegetation that surrounds them has the potential to draw carbon from the atmosphere and hence lessen the growth in carbon levels caused by human activity. The 2019 report by the Intergovernmental Panel on Climate Change on climate change and land has highlighted the role that carbon sequestration by soils could play in greenhouse gas mitigation (Section 4.9.4 IPCC, 2019).

    Finally, soils of all types have been extensively affected by resource extraction activities throughout western Canada. In Alberta alone, there are 422,000 km of oil and gas pipelines, 343,000 well sites (176,000 active wells, 90,000 inactive wells, and 77,000 abandoned wells) and 895 km2 have been disturbed by surface mining for oil sand production (as of 2013); oil sand tailing ponds and associated structures totaled 220 km2. (Sources: Agdex 878-4; Alberta Energy–Oil & Gas Liabilities Management; and Alberta Energy–Oil Sands, Coal and Mineral Operations). In all cases, legislation requires that the sites be reclaimed by replacing soil and re-establishing vegetation on the disturbed site so it can support activities similar to those it could have supported before it was disturbed. In situations where contamination has occurred the soils must be remediated (or cleaned up) to meet specific soil and groundwater standards. All of these steps require knowledge of soil properties and soil distribution, ensuring a continuing role for soil scientists form decades to come.


    Soil surveys in the Prairie Provinces can be queried on-line at the following sites:

    Saskatchewan: sksis
    Alberta: AGRASID

    Soil information (surveys, CLI maps, historic publications, Canadian System of Soil Classification) is available on-line through the Canadian Soil Information Service (CanSIS) of Agriculture and Agri-Food Canada. An index to CANSIS can be found at:

    Provincial-scale Canada Land Inventory maps are available at:

    Field Guides for Forest Ecosite Classification


    1. Explain why the carbonate content of Prairie soils generally decreases from a high in central Manitoba to a low in central Alberta.
    2. Why do Chernozemic soils occur as far north as Grand Prairie in Alberta (see Chapter 8, Figure 8.1)?
    3. Looking at Figure 10.3 – on what parent materials south of the Canadian Shield would you expect to find soils of the Vertisolic order?
    4. Based on the material presented in Chapter 10, rank the following four soils in terms of their ability to support crop growth from highest to lowest: Black Chernozem, Gray Luvisol, Humic Vertisol and Solodized Solonetz. Briefly explain your ranking.
    5. What are the four main soil great groups found on the Canadian Shield in the Prairie Provinces (see Figure 10.1)? Which of the four great groups is “out of place” on the Shield and why is it found there?
    6. What secondary soil properties reduce the CLI class for agriculture soils to class 5 or 6?
    7. Wetlands in the agricultural zone are often drained for agricultural purposes. What soil order is most common in these wetlands and what are two important ecosystem services that they provide?


    Anderson, D.W. 2010a. Vertisolic soils of the Prairie Region. Prairie Soils and Crops Journal 3: 29-36. Available at:

    Anderson, D. 2010b. Solonetzic soils of the Prairie region. 2010. Prairie Soils and Crops Journal 3: 65-72. Available at:

    Anderson, D.W. and Cerkowniak, D. 2010. Soil formation in the Canadian Prairie region. Prairie Soils and Crops Journal 3: 57-64. Available at:

    Bedard-Haughn, A. 2010. Prairie wetland soils; Gleysolic and Organic. Prairie Soils and Crops Journal 3: 9-15. Available at:

    Bedard-Haughn, A. 2011. Gleysolic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 763-779.

    Brierly, J.A., Stonehouse, H.B., and Mermut, A.R., 2011. Vertisolic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 903-916.

    Fox, C.A. and Tarnocai, C. 2011. Organic soils of Canada: Part 2. Upland Organic soils. Can. J. Soil Sci. 91: 823-842.

    Fuller, L. 2010. Chernozemic soils of the Prairie region of Canada. Prairie Soils and Crops Journal 3: 37-45. Available at:

    Intergovernmental Panel on Climate Change. 2019. Chapter 4: Land Degradation. IPCC Special Report on Climate Change and Land. Available at:

    Kroetsch, D.J., Geng, X., Chang, S.X., and Saurette, D.D. 2011. Organic soils of Canada: Part 1. Wetland Organic soils. Can. J. Soil Sci. 91: 807-822.

    Lavkulich, L.M. and Arocena, J.M. 2011. Luvisolic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 781-806.

    Macyk, T.M., Ellis, J.G., Michalyna, W., and Smith. R.E. 1978. Guidebook for a tour across the southern portion of the Interior Plains of Western Canada Tour 11. 11th Congress International Society of Soil Science. Edmonton Alberta June 1978. Available at:

    Michalyna, W., Smith, R.E., Ellis, J.G., and Macyk, T.M. 1978. Guidebook for a tour across the southern portion of the interior plains of western Canada from Winnipeg manitoba to Edmonton Alberta. Tour 2. 11th Congress International Society of Soil Science. Edmonton Alberta June 1978. Available at:

    Miller, J.J. and Brierly, J.A. 2011. Solonetzic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 889-902.

    Pennock, D.J., Bedard-Haughn, A., and Viaud, V. 2011. Chernozemic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 719-747.

    Pettapiece, W., Robertson, J., and Anderson, D. 2010. Cultivated gray Luvisol soils of the Prairie region. Prairie Soils and Crops Journal 3: 73-83. Available at:

    Prairie Farm Rehabilitation Administration. 2000. Prairie Agricultural Landscapes. A Land Resource Review . PFRA, Regina. pp. 180.

    St. Arnaud, R. J. 1976. Pedological aspects of glacial tills. Pages 133-155 in R.F. Legget, ed. Glacial Till. Royal Society of Canada, Ottawa, ON.

    Sanborn, P., Lamontagne, L., and Hendershot, P. 2011. Podzolic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 843-880.

    Smith, C.A.S., Webb, K.T., Kenney, E., Anderson, A., and Kroetsch, D. 2011. Brunisolic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 695-717.

    Soil Classification Working Group. 1998. The Canadian System of Soil Classification. 3rd Edition. Agriculture and Agri-Food Canada. Publ. 1646 (Revised). 187 pp. Available at:

    Tarnocai, C. and Bockheim, J.G. 2011. Cryosolic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 749-762.

    Thorpe, J. and Anderson, D. 2010. Soils of the rangelands in the Prairie region. Prairie Soils and Crops Journal 3: 46-56. Available at:

    VandenBygaart, A.J. 2011. Regosolic soils of Canada: Genesis, distribution and classification. Can. J. Soil Sci. 91: 881-887.


    Soil surveys in the Prairie Provinces can be accessed on-line at the following sites:

    Saskatchewan: sksis

    Alberta: AGRASID


    Canadian Soil Information Service (CanSIS) of Agriculture and Agri-Food Canada:

    Soil information (surveys, CLI maps, historic publications, Canadian System of Soil Classification) is available on-line through CanSIS. An index to CANSIS can be found at:

    Provincial-scale Canada Land Inventory maps are available at:

    About the Author

    Daniel J. Pennock, Professor Emeritus, Department of Soil Science, University of Saskatchewan

    Dan Pennock (licensed under a CC-BY-NC-ND license)

    Dan Pennock is a Professor Emeritus (or, more simply, a retired professor) of the Department of Soil Science at the University of Saskatchewan. His research career focused on how soils are shaped by their place in the landscape and by the processes (like erosion or water movement) that occur in landscapes. He taught courses in many areas of soil science and geography, and his love of teaching was recognized by the university with a Master Teacher award in 2006. He was made a Fellow of the Canadian Society of Soil Science in 2010. Since his retirement he has collaborated on a number of projects on sustainable management of soils with the Global Soil Partnership of the Food and Agriculture Organization of the United Nations.

    This page titled 2.2: Soils of the Prairie Provinces is shared under a CC BY-NC 4.0 license and was authored, remixed, and/or curated by Canadian Society of Soil Science via source content that was edited to the style and standards of the LibreTexts platform; a detailed edit history is available upon request.