Hydrogeology Mapping of

NTS Mapsheet Saskatoon 73B

Prepared for:

M1890-1030109 April 2011

Hydrogeological Mapping of the Saskatoon 73B Area April 2011

TABLE OF CONTENTS 1.0 INTRODUCTION ...... 1 1.1 Scope ...... 1 2.0 BACKGROUND ...... 2 2.1 Study Area ...... 3 2.2 Climate ...... 5 2.3 Topography and Drainage ...... 5 2.4 Land Use ...... 7 3.0 METHODOLOGY ...... 9 3.1 Stratigraphic Data Processing for Mapping ...... 9 3.1.1 Stratigraphic Mapping (Interpretation) ...... 10 3.2 Stratigraphic Database and Mapping Borehole Database ...... 11 3.3 Areal Limit and Aquifer Vulnerability Index Maps ...... 11 3.3.1 Areal Limit Determination ...... 12 3.3.2 Aquifer Vulnerability ...... 12 3.4 Groundwater Quality Data ...... 17 3.5 Hydraulic Properties ...... 17 3.6 Water Level Data ...... 19 3.7 Groundwater and Surface Water Withdrawal Data ...... 19 3.8 Groundwater Availability ...... 20 4.0 STRATIGRAPHY ...... 21 4.1 Regional Geological Setting ...... 21 4.2 Bedrock Deposits ...... 24 4.2.1 The Lea Park Formation ...... 24 4.2.2 The Judith River Formation ...... 25 4.2.3 The Bearpaw Formation ...... 25 4.3 Preglacial Drift Deposits ...... 26 4.3.1 The Empress Group ...... 26 4.4 Quaternary Drift Deposits ...... 27 4.4.1 The Sutherland Group ...... 27 4.4.2 The Saskatoon Group ...... 30 5.0 HYDROGEOLOGY ...... 31 5.1 The Judith River Aquifer ...... 34 5.1.1 Hydraulic Properties ...... 34 5.1.2 Groundwater Flow ...... 34 5.1.3 Groundwater Availability ...... 35 5.1.4 Groundwater Quality ...... 35 5.1.5 Groundwater Vulnerability ...... 35 5.2 The Ardkenneth Aquifer ...... 37 5.2.1 Hydraulic Properties ...... 37 5.2.2 Groundwater Flow ...... 37 5.2.3 Groundwater Availability ...... 37 5.2.4 Groundwater Quality ...... 37 5.2.5 Groundwater Vulnerability ...... 37 5.3 The Cruikshank Aquifer ...... 39 5.3.1 Groundwater Flow ...... 39 5.3.2 Groundwater Availability ...... 39 5.3.3 Groundwater Quality ...... 39 5.3.4 Groundwater Vulnerability ...... 39 5.4 The Empress Group Aquifer ...... 39 5.4.1 Hydraulic Properties ...... 40

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5.4.2 Groundwater Flow ...... 40 5.4.3 Groundwater Availability ...... 43 5.4.4 Water Quality ...... 43 5.4.5 Groundwater Vulnerability ...... 45 5.5 The Mennon Aquifer ...... 45 5.5.1 Hydraulic Properties ...... 45 5.5.2 Groundwater Flow ...... 45 5.5.3 Groundwater Availability ...... 45 5.5.4 Groundwater Quality ...... 46 5.5.5 Groundwater Vulnerability ...... 46 5.6 The Lower Dundurn Aquifer ...... 46 5.6.1 Hydraulic Properties ...... 46 5.6.2 Groundwater Flow ...... 46 5.6.3 Groundwater Availability ...... 48 5.6.4 Groundwater Quality ...... 48 5.6.5 Groundwater Vulnerability ...... 48 5.7 The Upper Dundurn Aquifer ...... 48 5.7.1 Hydraulic Properties ...... 50 5.7.2 Groundwater Flow ...... 50 5.7.3 Groundwater Availability ...... 51 5.7.4 Groundwater Quality ...... 51 5.7.5 Groundwater Vulnerability ...... 52 5.8 The Warman Aquifer ...... 54 5.8.1 Hydraulic Properties ...... 54 5.8.2 Groundwater Flow ...... 54 5.8.3 Groundwater Availability ...... 54 5.8.4 Groundwater Quality ...... 54 5.8.5 Groundwater Vulnerability ...... 54 5.9 The Lower Floral Aquifer ...... 56 5.9.1 Hydraulic Properties ...... 56 5.9.2 Groundwater Flow ...... 56 5.9.3 Groundwater Availability ...... 57 5.9.4 Groundwater Quality ...... 58 5.9.5 Groundwater Vulnerability ...... 58 5.10 The Upper Floral Aquifer ...... 58 5.10.1 Hydraulic Properties ...... 58 5.10.2 Groundwater Flow ...... 60 5.10.3 Groundwater Availability ...... 61 5.10.4 Groundwater Quality ...... 64 5.10.5 Groundwater Vulnerability ...... 64 5.11 The Battleford Aquifer ...... 64 5.11.1 Hydraulic Properties ...... 64 5.11.2 Groundwater Flow ...... 67 5.11.3 Groundwater Availability ...... 67 5.11.4 Groundwater Quality ...... 68 5.11.5 Groundwater Vulnerability ...... 68 5.12 The Surficial Aquifer ...... 68 5.12.1 Hydraulic Properties ...... 68 5.12.2 Groundwater Flow ...... 68 5.12.3 Groundwater Availability ...... 71 5.12.4 Water Chemistry ...... 71

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5.12.5 Groundwater Vulnerability ...... 73 6.0 CLOSURE ...... 74 7.0 DISCLAIMER ...... 75 8.0 REFERENCES ...... 76

APPENDICES Appendix A – Stratigraphic Chart Appendix B – Borehole Locations and Cross-Section Map Appendix C – Stratigraphic Cross-Sections Appendix D – Stratigraphic Database Appendix E – Structure Contour Maps Appendix F – Thickness and Areal Limit Maps Appendix G – Aquifer Vulnerability Maps

LIST OF FIGURES Figure 2.1 – Location of Saskatoon 73B area...... 4 Figure 2.2 – Regional hydrological features and watersheds...... 6 Figure 2.3 – Land use in the Saskatoon 73B area...... 8 Figure 4.1 – Borehole log SHT Sutherland Overpass No.4 (210624)...... 28 Figure 5.1 – Major preglacial aquifer boundaries of Saskatchewan...... 33 Figure 5.2 – Piper Plot groundwater chemistry of the Judith River Aquifer (Kjr) ...... 36 Figure 5.3 – Piper Plot groundwater chemistry of the Ardkenneth Aquifer (Kba) ...... 38 Figure 5.4 – Hydrograph SWA Duck Lake 2 (34715)...... 41 Figure 5.5 – Hydrograph for SWA Blucher No.3 (112761)...... 42 Figure 5.6 – Hydrograph for SWA Vanscoy (32338)...... 42 Figure 5.7 – Piper Plot groundwater chemistry results of the Empress Group Aquifer (QTe)...... 44 Figure 5.8 – Piper Plot groundwater chemistry results of the Mennon Aquifer (Qm-s)...... 47 Figure 5.9 – Piper Plot groundwater chemistry results of the Lower Dundurn Aquifer (Qd-ls)...... 49 Figure 5.10 – Hydrograph for SWA Warman #1 (32049)...... 50 Figure 5.11 – Hydrograph for SWA Warmam #2 (32050)...... 51 Figure 5.12 – Hydrograph for SWA Haque (34663)...... 52 Figure 5.13 – Piper Plot groundwater chemistry results of the Upper Dundurn Aquifer (Qd-us)...... 53 Figure 5.14 – Piper Plot groundwater chemistry results of the Warman Aquifer (Qw-s)...... 55 Figure 5.15 – Hydrograph for SWA Blucher No.4 (31403)...... 57 Figure 5.16 – Piper Plot groundwater chemistry results of the Lower Floral Aquifer (Qf-ls)...... 59 Figure 5.17 – Hydrograph for SWA Dalmeny (32183)...... 61 Figure 5.18 – Hydrograph for SWA Saskatoon (31803)...... 62 Figure 5.19 – Hydrograph from Silverspring MW21...... 62 Figure 5.20 – Hydrograph from Silverspring MW10...... 63 Figure 5.21 – Piper Plot groundwater chemistry results of the Upper Floral Aquifer (Qf-ms)...... 65 Figure 5.22 – Piper Plot groundwater chemistry results of the Upper Floral Aquifer (Qf-ms) Continued...... 66 Figure 5.23 – Hydrograph for SWA Agrium 43 (219583)...... 67 Figure 5.24 – Piper Plot groundwater chemistry results of the Battleford Aquifer (Qb-s)...... 69 Figure 5.25 – Hydrograph for SWA Duck Lake No. 1 (34714)...... 70 Figure 5.26 – Hydrograph for SWA Goodale Farm 9 (43769)...... 70 Figure 5.27 – Piper Plot groundwater chemistry results of the Surficial Stratified Deposits (Qssd)...... 72

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LIST OF TABLES Table 3.1 – Hydraulic conductivities for aquitard units used in AVI calculation...... 14 Table 3.2 – AVI ratings and codes...... 16 Table 3.3 – AVI applied to the Saskatoon 73B mapsheet...... 16 Table 3.4 – Typical hydraulic conductivities of hydrostratigraphic units...... 18 Table 3.5 – Storage properties for hydrostratigraphic units...... 18 Table 3.6 – Groundwater allocations in the Saskatoon 73B area...... 20

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1.0 INTRODUCTION This document provides the results of the hydrogeological mapping of the 1:250,000 NTS mapsheet Saskatoon 73B (Mapsheet 73B) area completed by MDH Engineered Solutions Corp. (MDH) on behalf of the Saskatchewan Watershed Authority (SWA), in cooperation with the Saskatchewan Research Council (SRC). The work on the shallow stratigraphy of the area has been ongoing for decades; however, the mapping of this area has never been completed formally. Formal mapping of this area began in November 2009 as a pilot project to establish standards for a subsequent province wide mapping effort. The Saskatchewan Watershed Authority had three broad objectives for the pilot project: 1. Hydrogeological mapping of Mapsheet 73B; 2. Development of standard mapping procedures and processes that are to be applied across the province; and 3. Exploration of knowledge products and their practicability.

1.1 Scope The general scope of the project was to complete geological, hydrogeological, and hydrostratigraphic mapping of Mapsheet 73B, as well as outlining the recommended procedures to complete hydrogeological mapping. The detailed scope of the project (as outlined in the RFP) was to: 1. Design and develop a methodology for regional groundwater mapping and characterization for Saskatchewan. The SWA intends to apply the methodology as the minimum standard for province wide mapping. The consultant was asked to consider a forward-thinking mapping protocol (or “standard”) that duly considers the optimal use of all significant data (regardless of the source), the approaches and systems of neighbouring jurisdictions, current and future technologies, future trends and needs, and the specific nature of Saskatchewan; 2. Investigate the feasibility and usefulness of new knowledge products, particularly groundwater vulnerability and water availability mapping. Any new products were to provide reasonable results and be worth the effort before being applied province- wide; therefore, some trial-and-error was anticipated; 3. Concurrently, map the 1:250,000 NTS Saskatoon 73B mapsheet as the prototype to ultimately be used for the standards developed; 4. Recommend how data, information, and knowledge should be delivered to customers; 5. Cooperate with and assist the SRC to draft the procedure and standards for regional hydrogeologic mapping and characterization to apply across Saskatchewan; 6. Possibly participate in ensuring the continuity of mapping skills into the future by involving/mentoring SWA staff members (or other promising candidates); 7. Provide options/recommendations as to how mapping should be executed across the province; and 8. Provide options/recommendations as to how mapping should be maintained into the

M1890-1030109 Page 1 Hydrogeological Mapping of the Saskatoon 73B Area April 2011

future.

Two separate reports were produced by MDH as part of this pilot project: 1) a report on the hydrogeology of the Saskatoon 73B area, and 2) a procedures and protocols document on hydrogeological mapping in Saskatchewan. The procedures used for hydrogeological mapping of 1:250,000 NTS mapsheets in Saskatchewan, on behalf of the SWA, are presented in a separate report entitled the “Procedures for Regional Hydrogeological Mapping” (MDH, 2010a). This procedures document is complemented by the SRC report entitled “Geology and Groundwater of Southern Saskatchewan, Hydrogeological Mapping Protocol” (Schreiner, 2010). The hydrogeology of the Saskatoon 73B area, including areal limit maps, aquifer vulnerability maps, and cross-sections, are provided herein.

2.0 BACKGROUND The SWA is facing demand from the public and government agencies for expert knowledge on groundwater resources. Groundwater mapping provides the data required to establish the hydrogeological framework for a site or region. This knowledge can be used to focus supplemental environmental, hydrogeological, and geotechnical field investigations for a site, guide site exploration and development, provide preliminary indications of aquifer vulnerability to surface contaminants, and/or determine potential sources of groundwater. Built from available data, the hydrogeological framework provides the SWA, industry consultants, and the public with fundamental information on the groundwater resources in an area, facilitating development and allowing the SWA to effectively manage, sustain, and protect groundwater.

During the late 1960s, the SRC conducted a groundwater mapping program to delineate potential groundwater resources in the agricultural sector of Saskatchewan based on NTS mapsheets at 1:250,000 scale. This program was started by the Agriculture and Rural Development Agency (ARDA) and resulted in 20 maps and was ended in 1980. A map of the geology and groundwater resources of the Saskatoon (73B) area was prepared by Christiansen (1967a) as part of this program. This program established the foundation for hydrostratigraphic mapping in Saskatchewan and led to what is referred to as the First Generation Groundwater Maps (FGGM). The maps illustrated the spatial extent and distribution of potential bedrock aquifers and were typically accompanied by four geologic cross-sections.

As the Quaternary geology of Saskatchewan became better understood, it was possible to map groundwater resources within the glacial drift. The Second Generation Groundwater Maps (SGGM) was conducted in 1986 by the SRC and the SWA to update the FGGM. This was completed by further defining the bedrock geology and mapping the major aquifers within the glacial deposits as well as the near surface bedrock deposits. These maps were developed from some boreholes with cuttings samples, cores, and geophysical logs, and some with only geophysical logs, resulting in a relatively coarse resolution. The maps only illustrated the spatial extent, thickness, and distribution of bedrock and glacial aquifers and

M1890-1030109 Page 2 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 are considered hydrostratigraphic maps because they did not include information on the water quality, potential yield, or vulnerability of the aquifers. The second generation mapping program completed twenty NTS mapsheets covering the majority of southern Saskatchewan. However, the geology, stratigraphy, and hydrogeology of the Saskatoon (73B) mapsheet was never completed. The maps and cross-sections were scanned and posted on the SWA website.

In 2004, the SWA initiated development of the third generation groundwater mapping for southern Saskatchewan. These maps provided public information on the groundwater resources and illustrated the spatial extent, distribution, and depth to potential aquifers. Detailed stratigraphic cross-sections illustrating the bedrock and Quaternary stratigraphy were completed as part of the study. The Cypress Hills (72F), Prelate (72K), Swift Current (72J), and Wood Mountain (72G) mapsheets were completed as the initial stages of this mapping program (Maathuis and Simpson, 2007a,b,c, and d). Maps were produced on the ESRI ArcGIS platform and posted on the SWA website, along with the reports describing the regional geology and hydrogeology.

The SWA presently recognizes the need for better groundwater knowledge and better public access to reliable data. The SWA also recognizes that without a current mapping plan, Saskatchewan risks losing key information and expertise in the near future. A new mapping program was therefore initiated by the SWA using the 1:250,000 NTS Saskatoon (73B) mapsheet as the pilot project to establish mapping standards and a subsequent province wide mapping effort. The SWA plans to run this program for four years initially and will provide the basic tools to manage groundwater and for reinvestment in the required expertise. The mapping program will provide a necessary update to the present understanding of Saskatchewan’s groundwater resources. It will also assist in the development of modern water allocation policies and identify areas susceptible to groundwater contamination. Concurrently, a new data management system has been utilized to better facilitate groundwater knowledge-building and to greatly improve both internal efficiency and timely dissemination of information to the public. This will be done, in part, by providing online information pertaining to southern Saskatchewan’s groundwater resources via the SWA website.

On 9 October 2009, MDH provided a proposal to the SWA to complete regional hydrogeological mapping of the Mapsheet 73B. MDH was commissioned to complete this work in November 2009. The primary output of the project is the ESRI ArcGIS databases and maps produced as part of this study. This report provides an accompanying overview of the hydrogeology of the Saskatoon 73B area.

2.1 Study Area The 1:250,000 NTS mapsheet Saskatoon 73B encompasses an approximate area of 15,109 km2, as shown in Figure 2.1.

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SQUARE HILL HATHERLEIGH BRIGHTHOLME LEASK MACDOWALL ALB RAVENHEAD ERTA BA MAYFAIR LORENZO ALDINA MANITO SILVER GROVE GARTHLAND SASKATCHEWAN GREEN CANYON REDFIELD WHITKOW OSCAR LAKE 324 MARCELIN 378 ALTICANE

12 TITANIC

BLAINE LAKE 212 KEATLEY CARLTON DUCK LAKE 0 TALLMAN ST-LAURENT-GR0 ANDIN 0 0 0 0 , KRYDOR , 0 0 5 5 8 8 , REDBERRY , 5 225 5 40 HAFFORD SPEERS BATOCHE RICHARD HAFFORD LAIRD LILAC DENHOLM 376 PETROFKA 312 OROLOW ROSTHERN RUDDELL WALDHEIM FISH CREEK 340 MAYMONT REDBERRY PARK GREAT DEER

BALJENNIE 16 HAGUE FIELDING HEPBURN HAGUE ALVENA CHORTITZ LANIWCI SPINNEY HILL GRUENTHAL RADISSON BLUMENTHAL SCHOENWEISE HOCHSTADT RADISSON MENNON NEUANLAGE SMUTS SONNINGDALE BORDEN 41 PRINCE ALBERT LANGHAM OSLER 0 0 0 0 0 0

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4 ENVIRON

MONARCHVALE BERGHEIM 11 YORKTON SASKATOON DIEFENBAKER INTERNATIONAL AIRPORT ASQUITH 16 DUNFERMLINE 14 SASKATOON 5 ST-DENIS MOOSE JAWREGINA SWIFT CURRENT BIGGAR GRANDORA BIGGAR JUNIATA PERDUE KINLEY 316 KEPPEL WEYBURN LENEY 7 d

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APPROXIMATE CLIMATE a SASKATOON 73B MAPSHEET AREA c o

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URBAN MUNICIPALITIES D X M _

LOCATION OF SASKATOON 73B AREA B 3

Notes: 7 _

SCALE AS SHOWN DATE 0 9

1. COORDINATE SYSTEM: NAD 1983 UTM ZONE 13N 8 1 M _ 2. CLIMATE STATION DATA OBTAINED FROM DESIGN BY G. POTTER, M.Sc., P.Eng. 14-APR-11 PRODUCED BY PROJECT No. M1890-1030009 FIG. No. 2.1 A W S SASKATCHEWAN ENVIRONMENT. \ A W

DRAWN BY 14-APR-11 DRAWING No. S 3. ELEVATION SCALES FOR PROVINCIAL VIEW DIFFER S. LONG, GIS Cert. \ : L

:

M1890-21-2 h FROM DETAIL VIEW AS INDICATED ABOVE. t APPROVED BY A. KARVONEN, M.Sc., P. Eng., P. Geo. 14-APR-11 a P Hydrogeological Mapping of the Saskatoon 73B Area April 2011

2.2 Climate Based on the modified Köppen classification, the Saskatoon 73B area has a continental climate characterized by hot summers, cold winters, and little rainfall. While there are more weather stations than shown on Figure 2.1 (http://climate.weatheroffice.gc.ca), only climate stations with averages determined for an approximate history between 1971 and 2000 were used in this report.

The average annual precipitation ranges from 316.5 mm/yr (Leney) to 408.6 mm/yr (Hague) with approximately 21% to 27% of that in the form of snowfall. Throughout the year the highest level of precipitation generally occurs during the months from May, June, and July. It is noted that the Leney climate station is located approximately 24 km south of the Town of Leney, immediately outside the limits of Figure 2.1

The annual average temperatures measured at the weather stations ranges between 1.3oC (Hafford) to 2.3oC (Leney). The month of January has the coldest temperatures on average, ranging from -15.9oC to -17.9oC, while July is the warmest month with average temperatures ranging between 17.2oC and 18.2oC in the Saskatoon 73B area.

Evaporation is one of the primary hydrological processes demanding most of the precipitation in the semi-arid regions of the Canadian prairies. Evapotranspiration is often described as an upward moisture flux from the land and the vegetation (Viessman and Lewis, 1996). In semi-arid regions, most precipitation is stored in the form of soil moisture and is eventually released as evapotranspiration.

Agriculture and Agri-Food Canada (2002) provides gross evaporation isolines based on a 30-year period for the Canadian prairies; the hydrology unit of the Prairie Farm Rehabilitation Administration (PFRA) created the gross evaporation map for Agriculture and Agri-Food Canada (AAFC). Based on the PFRA isolines, the mean annual gross evaporation for the area is estimated to range from approximately 800 mm to 920 mm in the northeast and the southwest corners, respectively.

2.3 Topography and Drainage Figure 2.2 shows the regional hydrological features and watersheds in the Saskatoon 73B area. The regional drainage basins identified in the study area are: 1) the North Saskatchewan River Watershed, 2) the South Saskatchewan River Watershed, and 3) the Eagle Creek Watershed. The North and the South Saskatchewan Rivers become the Saskatchewan River east of Prince Albert, SK. In the Saskatoon 73B area, topographic elevations range from approximately 430 metres above sea level (masl), in North Saskatchewan River Valley, to 754 masl, near Lizard Lake.

M1890-1030109 Page 5 300,000 330,000 360,000 390,000 420,000 0 0

0 SAND BEACH 0

0 DAMOUR 0 Legend , , 0 0 8 8 8 8 , , TOWN 5 HATHERLEIGH SQUARE HILL BRIGHTHOLME 5

IFFLEY LEASK MAJOR HIGHWAY ALDINA RAVENHEAD MACDOWALL WATERCOURSE MAYFAIR LORENZO 324 SILVER GROVE WATERBODY GREEN CANYON PADDLING GARTHLAND REDFIELD WHITKOW LAKE SASKATOON 73B MAPSHEET OSCAR LAKE MARCELIN URBAN MUNICIPALITIES 378 ALTICANE WATERSHED BOUNDARY GORDON ELEVATION (masl) LAKE 12 High : 780 Low : 430

TITANIC 212 ST-LAURENT- BLAINE LAKE R GRANDIN E KEATLEY IV 0 R CARLTON DUCK LAKE 0

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0 N 0 , KRYDOR TALLMAN A ST. ISIDORE- , 0 BLAINE LAKE 0 5 W DE-BELLEVUE 5 8 8 , 40 LAKES E 225 ,

5 REDBERRY H 5 C AT BRADA K S HAFFORD A S BATOCHE SPEERS H ST-JULIEN RICHARD T LAIRD REDBERRY R N O Notes: LILAC LAKE SOKAL DENHOLM 376 1. COORDINATE SYSTEM: NAD 1983 UTM ZONE 13N PETROFKA 312 ROSTHERN 2. DIGITAL ELEVATION MODEL DERIVED FROM CANADIAN OROLOW DIGITAL ELEVATION DATA (CDED) AND IS VERTICALLY RUDDELL WALDHEIM ACCURATE TO + OR – 10 METERS. FISH CREEK NORTH 340 S REDBERRY PARK GREAT DEER AS MAYMONT K 16 BALJENNIE A CARPENTER T C H EW 0 A 0 0 N FIELDING 0 0 0 , R HEPBURN , 0 IV 0 2 E 2 8 HAGUE 8 , R RADISSON ALVENA , 5 LAKE R 5 SPINNEY HILL CHORTITZ E LANIWCI V HOCHSTADT I RADISSON R BLUMENTHAL SCHOENWEISE N GRUENTHAL A W MENNON NEUANLAGE E H SMUTS C BORDEN T SONNINGDALE A K S 41 A S BUFFER LANGHAM OSLER H T LAKE LIZARD LAKE U DALMENY STRUAN O S PRUD'HOMME ABERDEEN 305 WARMAN 27 4 VONDA MARTENSVILLE

ARELEE 0 0

0 0 TITLE 0 0

, , REGIONAL HYDROLOGICAL 0 ENVIRON 0 9 9 7 7 , ,

5 5 FEATURES AND WATERSHEDS MONARCHVALE 73B NTS MAPSHEET 11 BERGHEIM PROJECT No. M1890-1030009 FIG. No. 2.2 d

WHITESHORE DRAWING No. M1890-24-23 x m

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300,000 330,000 360,000 390,000 420,000 APPROVED BY A. KARVONEN, M.Sc., P.Eng., P.Geo. 14-APR-11 P Hydrogeological Mapping of the Saskatoon 73B Area April 2011

2.4 Land Use Three ecoregions are present in the study area: the Boreal Transition, the Aspen Parkland, and the Moist Mixed Grassland (Acton et al., 1998). The Boreal Transition Ecoregion stretches across central Saskatchewan between the boreal forest to the north and the grasslands to the south. The Boreal Transition Ecoregion is composed of forest and farmland, marking the northern advance of arable agriculture and the southern extent of closed boreal forest. The most extensive land use in the study area is agriculture (Figure 2.3), with nearly 50% of the lands under cultivation, supporting crops of spring wheat and other cereals, oilseeds, and hay. Other land use activities in the ecoregion include forestry, hunting, fishing, and recreation. The natural habitat is dominated by mixed wood boreal forest, supporting a variety of tree species including trembling aspen, white spruce, black spruce, tamarack and jack pine. The understory vegetation varies from dense herbs and tall shrubs to a variety of grass species.

The Aspen Parkland Ecoregion extends from the southeast corner of the province to the Alberta border near Lloydminster. This region represents the transition zone between forested areas and grassland. The generally hummocky landscape is composed of aspen groves in moist areas and fescue grasslands in drier areas. Trembling aspen forests dominate the northern portion of the ecoregion and grasslands thrive in the southern extent of the area. The dominant land use is agriculture, with 80% of the ecoregion dedicated to cropland, producing cereals and oilseeds or planted to a perennial forage crop. Land that is not suitable for crops is often used as pasture land to support livestock. This ecoregion is home to large number of urban city centers, towns, and villages which dedicate surrounding lands to residential development and light industry.

The Moist Mixed Grassland Ecoregion cuts through the southern portion of Saskatchewan from Estevan to Saskatoon and straight west to the Alberta Border. This area represents the northern most extent of open grassland. Wheatgrass and spear grass are the dominant grass species in the region with trembling aspen residing in areas around wetlands. The ecoregion supports 55% of Saskatchewan’s population, creating a landscape for a variety of land-uses. Agriculture is the dominant land use in the ecoregion with 80% of the land under cultivation. Crops include spring wheat and other cereal grains, with oilseed becoming an important contributor to total crop production. Areas that are not suitable for cultivation are often used as pasture land for livestock. Mining is a large industry throughout the ecoregion.

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Legend NATPSP SRAOSXKIAMTAOTOE NN T73SB S MASAKPASTHOEOENT A7R3BE AMAPSHEET CCUULLITITIVIVAATTEEDD L LAANNDD HHAAYY C CRROOPP ( F(FOORRAAGGEE) ) NNAATTIVIVEE D DOOMMININAANNTT G GRRAASSSSLLAANNDD TTAALLL S SHHRRUUBB PPAASSTTUURREE ( S(SEEEEDDEEDD G GRRAASSSSLLAANNDD) ) HHAARRDDWWOOOODD O OPPEENN HHAARRDDWWOOOODD C CLLOOSSEEDD JAJACCKKPPININEE C CLLOOSSEEDD JAJACCKKPPININEE O OPPEENN SSPPRRUUCCEE C CLLOOSSEEDD 0 0 0 0 0 0 , , SSPPRRUUCCEE O OPPEENN 0 0 5 5 8 8 , ,

5 5 MMIXIXEEDD W WOOOODD TTRREEEEDD R ROOCCKK RREECCEENNTT B BUURRNN RREEVVEEGGEETTAATTININGG B BUURRNN CCUUTTOOVVEERR WWAATTEERRBBOODDYY MMAARRSSHH HHEERRBBAACCEEOOUUSS F FEENN MMUUDD/S/SAANNDD/S/SAALLININEE SSHHRRUUBB F FEENN ( T(TRREEEEDD S SWWAAMMPP) ) TTRREEEEDD B BOOGG OOPPEENN B BOOGG FFAARRMMSSTTEEAADD NNOO D DAATTAA OOTTHHEERR

Note 1. COORDINATE SYSTEM: NAD 1983 UTM ZONE 13N

0 0 2. SASKATCHEWAN SOUTH DIGITAL LAND COVER DATA 0 0 0 0 , , OBTAINED FROM SASKATCHEWAN INTERACTIVE, 0 0 0 0 8 8 , , SASKATCHEWAN MINISTRY OF ENVIRONMENT. 5 5

TITLE LAND USE IN THE SASKATOON 73B AREA

PROJECT No. M1890-103009 FIG. No. 2.3

DRAWING No. M1890-26-1 d x m . ) e

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d n a L (

1 0 - 6 2 - 0 9 8 PRODUCED BY 1 M \ D X M _ B 3 7 _ 0 9 8 1 M

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DRAWN BY J.S. BAILEY, B.A., GIS Cert. 14-APR-11 L

: h t A. KARVONEN, M.Sc., P.Eng., P.Geo. a 300,000 350,000 400,000 APPROVED BY 14-APR-11 P Hydrogeological Mapping of the Saskatoon 73B Area April 2011

3.0 METHODOLOGY MDH compiled and examined well, borehole, and hydrogeology related data from a number of sources to complete the hydrogeological mapping of the Saskatoon 73B area. The SWA and the SRC provided the majority of the information necessary to complete the mapping project. Additional sources were required to provide the full scope of hydrogeological work completed in the study area. Databases and data sources that were compiled for the Mapsheet 73B included: 1. Wells Database a. SWA Database b. SRC Wells Database 2. Log Data a. SWA borehole logs b. SWA library report borehole logs c. SRC auger borehole logs d. SRC borehole logs with geophysics e. SRC carbonate data f. Saskatchewan Ministry of Highways and Infrastructure (SMHI) historical borehole logs g. SMHI Geotechnical Database logs h. Saskatchewan Ministry of Energy and Resources (SMER) logs i. SMER stratigraphic database j. Petroleum Technology Research Centre (PTRC) database k. Selected private industry borehole logs 3. Water Quality Databases a. SWA Provincial Water Quality dataset b. SWA FoxPro Water Quality dataset c. Rural Water Quality Advisory Program (RWQAP) dataset 4. Licensed Groundwater Database 5. Hydrogeological Investigation Reports a. SWA Library b. Other public reports 6. Observation Well Water Levels 7. Community Water Use Database The procedures implemented in the collection and processing of these datasets is provided in “Procedures for Regional Hydrogeological Mapping” (MDH, 2010a).

3.1 Stratigraphic Data Processing for Mapping Following data compilation and processing, a total of 2,589 auger borehole logs, professional logs with geophysics, driller’s logs with geophysics, and PTRC database records were used to map the stratigraphic units in the Saskatoon 73B area. These records comprise the Mapping Dataset that contains tabulated boreholes and well information (Mapping Borehole

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Database) and the associated stratigraphy (Stratigraphic Database). All records are referenced with the SWA Water Well Drilling Record (WWDR) ID. The WWDR ID is used to identify boreholes in this report. It is noted that the used boreholes are not comprehensive, as not all of the existing boreholes are publically available. There is a vast amount of information in consulting reports for private industry that were not available.

3.1.1 Stratigraphic Mapping (Interpretation) Professional MDH hydrogeologists provided the stratigraphic interpretations for each borehole. The PTRC stratigraphic database was used for the stratigraphic interpretation of the deep exploration boreholes. No attempt was made to alter the provided picks in the PTRC database, even if they were suspect. Alteration of the deep PTRC data was beyond the scope of this study.

Appendix A provides the stratigraphic chart for hydrogeological mapping of the Saskatoon area and southern Saskatchewan. It also provides the stratigraphic chart for the Saskatoon 73B area. These charts provide the relative age, stratigraphy, generalized lithology, and a corresponding identification number (i.e. the identification number used to code each hydrostratigraphic unit). The references used to compile this stratigraphic chart are provided on the chart in Appendix A. Anybody doing hydrostratigraphic mapping in Saskatchewan is encouraged to study each of these references to assist in the development of the necessary knowledge and skills to do similar work in the province. The SRC report entitled “Geology and Groundwater of Southern Saskatchewan, Hydrogeological Mapping Protocol” (Schreiner, 2010) and the MDH report entitled “Procedures for Regional Hydrogeological Mapping” (MDH, 2010a), should also be studied prior to doing any geological or hydrogeological mapping in southern Saskatchewan.

The location and extent of the hydrostratigraphic units involves varying levels of uncertainty. Existing geological and hydrostratigraphic data can be fairly sparse. The majority of water wells in the area are privately drilled to support local farming operations. Many of these wells were not drilled to a stratigraphic marker (e.g. Upper Cretaceous bedrock shale) and/or do not have carbonate data. Stratigraphic interpretations completed without this information can be uncertain. Similarly, the majority of the lithologic descriptions on the boreholes were not created by a professional (i.e. no geologist, engineer, or technologist was on site to provide descriptions of the drill cuttings) and the lithology reported on the logs is based on driller’s descriptions, which, in the experience of MDH are often unreliable.

An interpretation of the stratigraphy at each borehole (i.e. a strip log) was created using the geophysical signatures supplemented with the driller’s or professional’s notes, as well as geotechnical soil testing and carbonate contents. While this is the most comprehensive interpretation of the stratigraphy and hydrogeology based on the available information; it is and will be subject to error. As a result of this uncertainty, the interpretations provided based on this data should not be used for decisions relating to a development or well installation without verification (i.e. confirmatory drilling). The compiled maps and

M1890-1030109 Page 10 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 cross-sections should only be used to provide the stratigraphic framework for the area and to make large-scale general decisions to guide site specific investigations. All interpretations should be completed by a professional geoscientist. 3.1.1.1 Stratigraphic Interpretation Methodology The principles described in the MDH (2010a) and the Schreiner (2010) reports were used to interpret the stratigraphy (i.e. make stratigraphic picks) at each borehole in the Stratigraphic Database. Stratigraphic cross-sections were created as an initial step in the stratigraphic interpretation process. In general, borehole logs with good geophysical signatures, lithologic descriptions, and those with supplemental data (especially carbonate contents) were used for the cross-sections. It is noted that there are areas where limited high quality data is available; in these areas, the best information available was used. Appendix B provides a map showing the boreholes used in this study and the cross-section locations created for the Saskatoon 73B area. Professional logs containing geophysical information to the top of the Lea Park Formation shale were preferred for the creation of the stratigraphic cross-sections across the study area. MDH (2010a) provides the procedure used to generate the stratigraphic cross-sections.

The interpretation is meant to provide the overall stratigraphic framework for the area and to provide general information in which to focus more detailed investigations. Site specific drilling will provide more reliable data for any potential location within the mapsheet. Although the interpretation will be subject to errors, it provides a general hydrostratigraphic framework for the Saskatoon 73B area, and can be used to aid high level decisions that require knowledge of the shallow stratigraphy and hydrogeology. The interpreted stratigraphic picks were input into the Stratigraphic Database, and the borehole and well information was input into the Mapping Borehole Database, concurrently during the creation of stratigraphic cross-sections and associated maps.

3.2 Stratigraphic Database and Mapping Borehole Database A Stratigraphic Database and Mapping Borehole Database were created to map the hydrogeology of the study area, as described in MDH (2010a). These databases were then converted to an Arc Hydro compatible database and imported into the Arc Hydro Groundwater Data Model (AHGDM). The AHGDM is based on the ESRI Geodatabase (GDB) format such that the compiled and interpreted information can be accessed via the internet. The “Procedures for Regional Hydrogeological Mapping” (MDH, 2010a) provides details on the creation and conversion of these databases into the GIS based AHGDM, such that the information could be used to generate areal limit maps of the mappable stratified deposits, correlate water chemistry and groundwater allocation data to hydrostratigraphic units, and create aquifer vulnerability maps for the Saskatoon 73B study area.

3.3 Areal Limit and Aquifer Vulnerability Index Maps Areal limit and Aquifer Vulnerability Index (AVI) maps were created for each of the mappable stratified deposits above the Lea Park Formation. Areal limit and thickness maps are an

M1890-1030109 Page 11 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 important resource for groundwater management and siting potential developments. The only defendable way to properly interpret and map complex glacial stratigraphy is to use geologic principals and established formally defined stratigraphic divisions. This means mapping formal stratigraphic units (Formations, Groups, etc.) and not grouped hydrostratigraphic divisions based on material properties. Following reviews and discussions with the external technical guidance committee it was decided that stratified units would be mapped with no emphasis on whether they were aquifers or aquitards. This decision was made because the local variability of these deposits can result in both aquifer and aquitard units being present over short distances. As it result, it was determined that further subdivision of the stratified deposits could be misleading depending on the sophistication of the user and the purpose for the use of the knowledge product. The GIS based platform would enable users to readily access actual borehole logs during any query to determine what the composition of individual stratified deposits are at any location. The procedures used to create these areal limit and AVI maps is outlined in the MDH (2010a) report.

3.3.1 Areal Limit Determination Areal limit determination is the process of analyzing the interpreted stratigraphic picks on borehole logs to determine the 2D (areal) and 3D extents of the respective hydrostratigraphic units. This process can be completed manually by “hand contouring” or through an interpolation process using a technique such as natural neighbour to produce a representative surface. This representative surface can then be compared to other horizons (such as the existing topography) to determine overlaps which are removed (clipped) where necessary.

The SWA requested that all contouring be completed using automated computerized methods and that no contouring be completed by hand, such that a web-based Arc Hydro Groundwater Data Model (AHGDM) could be established. It is recognized that computerized determination of the 2D areal limits of mappable stratified deposits will lead to some misrepresentation of the areal extent of these sediments (especially in vicinity of channel features). Contouring by hand provides a significantly better product as geological and geomorphological processes can be used to guide the process. Hand contouring is time consuming and requires re-contouring by hand whenever new data is added. Due to these limitations, a computerized contouring package was considered more desirable for this process. The cross-sections and areal limit maps may not match exactly because the cross- sections were created by hand and the areal limit maps were generated using an automated computerized process.

3.3.2 Aquifer Vulnerability Construction and operation of a facility (industrial, agricultural, etc.) can result in significant local effects on the groundwater flow system and can pose a threat to the quality and quantity of subsurface groundwater. These impacts can be reduced through optimizing the

M1890-1030109 Page 12 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 location and/or design of the facility. The vulnerability of subsurface aquifers due to a facility will be a direct function of: 1. the properties of the contaminant; 2. the level of natural containment of the sediments(i.e. aquitard thickness); and 3. the design of the waste storage facility. Protecting the quality of groundwater from contamination is becoming a priority throughout the world as remediation of polluted groundwater and development of clean-up technologies is highly expensive. The risk of pollution to groundwater resources from industrial expansion has resulted in the need to map the vulnerability of these “freshwater” resources on large scales. Aquifer vulnerability can be defined as follows: Intrinsic (or natural) vulnerability is the vulnerability solely dependent on the characteristics of an aquifer and the overlying soil and geological materials. It differs from the specific (or integrated) vulnerability in that the latter includes the potential impact(s) of specific land uses or contaminants (Vrba and Zaporozec, 1994).

3.3.2.1 Aquifer Vulnerability Index (AVI) Methodology Various methods have been used to map aquifer vulnerability, but there is no universally accepted method to date. Consequently, interpretation of vulnerability maps requires an understanding how they are created. While there are various methods, the ultimate objective of vulnerability mapping is protecting the quality of groundwater by means of the development of land use guidelines or hazardous chemical restrictions. This can involve combinations of: 1) protection of the entire aquifer, 2) protection of vulnerable areas, and/or 3) protection of well capture areas (i.e. well head protection). Protection of an entire aquifer might be desirable from a point of view of protecting present and future water supplies, but may not be feasible in all cases. Compromises that involve some form of well head protection and protection of the recharge zone are typically required and the area to be protected may extend beyond the boundaries of the aquifer. In many countries this has lead to defining zones around a well head based on travel time considerations.

Regional scale aquifer vulnerability maps are useful as initial screening tools for land use management. Local and more detailed studies are required to assess the potential impact on a groundwater resource by a specific land use. For this investigation, a modified aquifer vulnerability index (AVI) was used. This AVI was modified from the van Stempvoort et al. (1992 and 1993) method that was developed as a tool for regional-scale mapping of the vulnerability of aquifers to contamination from potential sources at or near the ground surface. The method was modified to provide vulnerability maps of multiple stacked aquifers.

The AVI is based on two parameters: 1. the thickness (D) of the confining aquitard layer above an aquifer, and

2. the vertical hydraulic conductivity (Kv) of the confining aquitard layer.

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These two parameters can be combined into a single factor, the hydraulic resistance:

D c = [1] K v

where: c = vertical hydraulic resistance (y) D = thickness of confining layer overlying aquifer (m) Kv = vertical hydraulic conductivity (m/y)

For a sequence of layers, the total resistance to flow becomes the sum of the c values of individual aquitard layers. It is assumed all surficial stratified deposits and intertill deposits are aquifers and have no vertical resistance (this is assumed to keep the calculation conservative). This means only the till and shale units (aquitards) are used in calculation of the total vertical resistance. The total vertical resistance is calculated as follows:

n D -8 c = i x 3.1688x10 [2] T ∑ K i=1 vi

where: CT = Total vertical resistance (y)

Di = Thickness of layer i (m) K = Vertical hydraulic conductivity of layer i (m/s) vi n = Number of layers -8 note: 3.1688x10 provides conversion of CT conversion from seconds to years (there are 3.15576x107 seconds per year)

The hydraulic conductivities used for this investigation were based on literature values and engineering judgment, with conservative (high) hydraulic conductivities for the shallow aquitard deposits due to their control over the vulnerability of shallow aquifer systems. The assumed hydraulic conductivities for each confining hydrostratigraphic unit are provided in Table 3.1.

Table 3.1 – Hydraulic conductivities for aquitard units used in AVI calculation.

Group Aquitard Unit Aquitard Abbreviation Hydraulic Conductivity (m/s) Saskatoon Group Battleford Till Qb-t 1.0E-07 Upper Floral Till Qf-ut 1.0E-08 Lower Floral Till Qf-lt 1.0E-09 Basal Floral Till Qf-bt 1.0E-09 Sutherland Group Warman Till Qf-wt 1.0E-10 Upper Dundurn Till Qd-ut 1.0E-10 Lower Dundurn Till Qd-lt 1.0E-10 Basal Dundurn Till Qd-bt 1.0E-10 Upper Mennon Till Qm-ut 1.0E-10 Lower Mennon Till Qm-lt 1.0E-10 Bearpaw Formation Aquadell Member Shale Kbaq 1.0E-11 Snakebite Member Shale Kbs 1.0E-11 Beachy Member Shale Kbby 1.0E-11

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To facilitate plotting and contouring of the hydraulic resistance data, the AVI has been defined as:

AVI = Log10 (c) [3] The categories for AVI, and there corresponding vulnerability rating and mapping code, are provided in Table 3.2. Table 3.3 provides the values applied to the Saskatoon 73B area. These ratings and codes were used for mapping of the vulnerability of each of the stratified deposits. This assumes that each stratified deposit is comprised of aquifer material.

Contouring of AVI values will give the impression of lateral continuity of aquifers and gradation of the index. Neither lateral continuity nor gradation of the AVI values is realistic since hydrogeological settings can change over short distances. The AVI is an averaged property but vulnerability depends on local point values. The aquifer vulnerability mapping should only be considered a guide for the placement of contaminants and has a number of limitations, including: • The method assumes that the vulnerability of a mappable stratified deposit is calculated at a point based on overlying deposits at that location. It estimates vulnerability of a hydrostratigraphic unit based on vertical flow at a point source. It does not take into account vulnerability due to: a. potential aquifer connectivity in multiple stacked systems; b. vulnerability of the aquifer at any location due to lateral flow within the aquifer; c. the influence of complex geological structures (e.g. faulting) or unsaturated conditions, etc.; or d. anthropogenic influences (i.e. preferential conduits due to improperly grouted boreholes or wells). • The method ignores parameters such as: climate, hydraulic gradient, porosity, and water content of the porous media in favour of simple dependence on the two key variables. • The AVI values are determined from information that varies highly in detail and quality (e.g. if using the SWA water well driller’s database without quality control). • The AVI vulnerability classes have been arbitrarily selected based on engineering judgment and approximated hydraulic conductivities. • Saturated hydraulic conductivities are used for unsaturated sediments. Since the hydraulic conductivity of unsaturated sediments is less than that of saturated sediments, the calculated resistance is conservative. • Fracturing is only taken into account in the hydraulic conductivities of the upper Saskatoon Group tills. Fractures can increase hydraulic conductivity by several orders of magnitude. The AVI ratings should only be used as a guide and site specific data is required to properly assess the presence and vulnerability of any aquifer unit.

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Table 3.2 – AVI ratings and codes. Hydraulic Aquifer Vulnerability Index (Log C) Vulnerability Rating Vulnerability Color Codes 0 to 10 < 1 very high very high 10 to 100 1 to 2 high high 100 to 1,000 2 to 3 moderate moderate 1,000 to 10,000 3 to 4 low low > 10,000 > 4 very low very low

Table 3.3 – AVI applied to the Saskatoon 73B mapsheet.

Aquitard Hydraulic Thickness of Aquitard Group Aquitard Unit Abbreviation Conductivity (m/s) 1 m 2 m 3 m 4 m 5 m 6 m 7 m 8 m 9 m 10 m 15 m 20 m 25 m 30 m 35 m 40 m 45 m 50 m 60 m 70 m 80 m 90 m 100 m 120 m 140 m 160 m 180 m 200 m Saskatoon Group Battleford Till Qb-t 1.0E-07 0.0 0.0 0.0 0.1 0.2 0.3 0.3 0.4 0.5 0.5 0.7 0.8 0.9 1.0 1.0 1.1 1.2 1.2 1.3 1.3 1.4 1.5 1.5 1.6 1.6 1.7 1.8 1.8 Upper Floral Till Qf-ut 1.0E-08 0.5 0.8 1.0 1.1 1.2 1.3 1.3 1.4 1.5 1.5 1.7 1.8 1.9 2.0 2.0 2.1 2.2 2.2 2.3 2.3 2.4 2.5 2.5 2.6 2.6 2.7 2.8 2.8 Lower Floral Till Qf-lt 1.0E-09 1.5 1.8 2.0 2.1 2.2 2.3 2.3 2.4 2.5 2.5 2.7 2.8 2.9 3.0 3.0 3.1 3.2 3.2 3.3 3.3 3.4 3.5 3.5 3.6 3.6 3.7 3.8 3.8 Basal Floral Till Qf-bt 1.0E-09 1.5 1.8 2.0 2.1 2.2 2.3 2.3 2.4 2.5 2.5 2.7 2.8 2.9 3.0 3.0 3.1 3.2 3.2 3.3 3.3 3.4 3.5 3.5 3.6 3.6 3.7 3.8 3.8 Sutherland Group Warman Till Qf-wt 1.0E-10 2.5 2.8 3.0 3.1 3.2 3.3 3.3 3.4 3.5 3.5 3.7 3.8 3.9 4.0 4.0 4.1 4.2 4.2 4.3 4.3 4.4 4.5 4.5 4.6 4.6 4.7 4.8 4.8 Upper Dundurn Till Qd-ut 1.0E-10 2.5 2.8 3.0 3.1 3.2 3.3 3.3 3.4 3.5 3.5 3.7 3.8 3.9 4.0 4.0 4.1 4.2 4.2 4.3 4.3 4.4 4.5 4.5 4.6 4.6 4.7 4.8 4.8 Lower Dundurn Till Qd-lt 1.0E-10 2.5 2.8 3.0 3.1 3.2 3.3 3.3 3.4 3.5 3.5 3.7 3.8 3.9 4.0 4.0 4.1 4.2 4.2 4.3 4.3 4.4 4.5 4.5 4.6 4.6 4.7 4.8 4.8 Basal Dundurn Till Qd-bt 1.0E-10 2.5 2.8 3.0 3.1 3.2 3.3 3.3 3.4 3.5 3.5 3.7 3.8 3.9 4.0 4.0 4.1 4.2 4.2 4.3 4.3 4.4 4.5 4.5 4.6 4.6 4.7 4.8 4.8 Upper Mennon Till Qm-ut 1.0E-10 2.5 2.8 3.0 3.1 3.2 3.3 3.3 3.4 3.5 3.5 3.7 3.8 3.9 4.0 4.0 4.1 4.2 4.2 4.3 4.3 4.4 4.5 4.5 4.6 4.6 4.7 4.8 4.8 Lower Mennon Till Qm-lt 1.0E-10 2.5 2.8 3.0 3.1 3.2 3.3 3.3 3.4 3.5 3.5 3.7 3.8 3.9 4.0 4.0 4.1 4.2 4.2 4.3 4.3 4.4 4.5 4.5 4.6 4.6 4.7 4.8 4.8 Bearpaw Formation Aquadell Member Shale Kbaq 1.0E-11 3.5 3.8 4.0 4.1 4.2 4.3 4.3 4.4 4.5 4.5 4.7 4.8 4.9 5.0 5.0 5.1 5.2 5.2 5.3 5.3 5.4 5.5 5.5 5.6 5.6 5.7 5.8 5.8 Snakebite Member Shale Kbs 1.0E-11 3.5 3.8 4.0 4.1 4.2 4.3 4.3 4.4 4.5 4.5 4.7 4.8 4.9 5.0 5.0 5.1 5.2 5.2 5.3 5.3 5.4 5.5 5.5 5.6 5.6 5.7 5.8 5.8 Beachy Member Shale Kbby 1.0E-11 3.5 3.8 4.0 4.1 4.2 4.3 4.3 4.4 4.5 4.5 4.7 4.8 4.9 5.0 5.0 5.1 5.2 5.2 5.3 5.3 5.4 5.5 5.5 5.6 5.6 5.7 5.8 5.8

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3.4 Groundwater Quality Data Three separate water quality datasets were provided for Saskatoon 73B area, including: 1. SWA Provincial Water Quality dataset 2. SWA FoxPro Water Quality dataset 3. Rural Water Quality Advisory Program (RWQAP) dataset

These datasets were combined as discussed in the procedures manual (MDH, 2010a). Records without a WWDR ID were cross-referenced with the SWA Wells Database and a WWDR ID was populated where possible. The Water Quality Database was also cross referenced to the Mapping Borehole Database to assign completion horizons (stratigraphic units) for wells.

3.5 Hydraulic Properties Definition of the hydraulic properties (hydraulic conductivity, porosity, compressibility, and specific storage) of the hydrostratigraphic units, and their spatial distribution and connectivity, is essential for the understanding of aquifer vulnerability and groundwater availability. These properties are combined with the stratigraphy of a study area to describe the three- dimensional framework of aquifers and aquitards, and to formulate a 3D representation of the natural system.

Gravels and sands represent high hydraulic conductivity units (aquifers) in the study area. Tills, clays, and silts comprise the low hydraulic conductivity units (aquitards). The hydraulic conductivities for the hydrostratigraphic units are expected to fall within the ranges provided in Table 3.4. Pumping test results often report transmissivity, which is the hydraulic conductivity of an aquifer multiplied by its thickness.

Unlike hydraulic conductivity (where values range over many orders of magnitude), porosities tend to range from 5% to 50%. Porosity was estimated based on typical ranges for different lithologies as cited in the literature (Table 3.5). Porosity accounts for changes in storage in unconfined aquifers, but for confined aquifers, where the pore-space is fully saturated, changes in pore pressures and surface loads result in an elastic response in both the porous medium and the pore fluid. Specific storage is the volume of water released from a unit volume of confined media per unit decline in hydraulic head per unit thickness. Porosity and compressibility of both the porewater and the porous medium are related to specific storage as follows:

Ss = (α + nβ)γ w -1 where: Ss = specific storage [L ] α = compressibility of the soil matrix [F-1L2] -1 2 β = compressibility of water [F L ] n = porosity [ ] -3 γw = specific weight of water [FL ]

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Table 3.4 – Typical hydraulic conductivities of hydrostratigraphic units.

Hydrostratigraphy Hydraulic Lithology Hydraulic Conducitivity Behavior Lower Limit (m/s) Upper Limit (m/s) Surficial Stratified Deposits Aquifer/Aquitard Gravel >5x10-4 (1)(6)(8) Sand 2x10-7 (6)(8) 1x10-3 (2)(6)(8) Silt 1x10-7 (6)(8) 5x10-6 (6)(8) Clay 1x10-11 (1)(2)(6)(8) 1x10-6 (6)(8) Oxidized Saskatoon Group Till Poor Aquitard Till 1x10-10 (1)(3)(8) 3x10-6 (8) Unoxidized Saskatoon Group Till Aquitard Till 1x10-11 (1)(3)(8) 1x10-8 (8) Sutherland Group Till Till 1x10-11 (1)(4)(5)(8) 1x10-10 (8) Bearpaw Formation Shale Silt and Clay 3x10-8 (8) 3x10-12 (8) Lea Park Formation Shale Silt and Clay 3.8x10-12 (9) 3.8x10-10 (9) Saskatoon Group Aquifers Aquifer Gravel and Sand 1x10-6 (6)(8) 1x10-3 (6)(8) Gravel, Sand, Silt, Clay 1x10-8 (8) 5x10-4 (8) Sutherland Group Aquifers Aquifer Gravel and Sand 1x10-6 (6)(8) 1x10-3 (6)(8) Gravel, Sand, Silt, Clay 1x10-8 (8) 1.0x10-3 (8) Empress Group Aquifer Aquifer Gravel and Sand 1x10-5 (8)(9) 1x10-3 (6)(8) Gravel, Sand, Silt, Clay 1x10-9 (8) 1x10-3 (8) Bearpaw Formation Sands Aquifer Sand and Silt 1.2x10-5 (11) 5.8x10-5 (11) Sand, Silt, Clay 2x10-9 (6) 8x10-4 (6) Judith River Formation Aquifer Sand and Silt 1.9x10-6 (10) 1.7x10-5 (10) 1) Maathuis and van der Kamp (1994) 6) Freeze and Cherry (1979) 11) Maathuis and Simpson (2007) 2) Domenico and Schw artz (1998) 7) Maathuis and Schreiner (1982) 3) Ho and Barbour (1987) 8) Estimates based on MDH experience and testing on similar soils 4) Keller et al. (1988) 9) Misfiedt (1988) 5) Keller et al. (1989) 10) Kew en and Schneider (1979)

Table 3.5 – Storage properties for hydrostratigraphic units.

Hydrostratigraphy Hydraulic Lithology Soil Compressibility (m2/N) Porosity Limit (%) Behavior LL * UL * LL UL Surficial Stratified Deposits Aquifer Gravel 1.0x10-9 1.0x10-7 25 35 Aquifer Sand 1.0x10-9 1.0x10-7 25 40 Aquitard Silt 1.0x10-8 2.0x10-6 30 50 Aquitard Clay 1.0x10-8 2.0x10-6 40 50 Oxidized Saskatoon Group Till Poor Aquitard Till 5.2x10-9 2.0x10-6 20 45 Unoxidized Saskatoon Group Till Aquitard Till 5.2x10-9 2.0x10-6 20 50 Sutherland Group Till Aquitard Till 5.2x10-9 2.0x10-6 20 50 Upper Cretaceous Shale Aquitard Silt and Clay 5.2x10-9 2.0x10-6 5 30 Battleford Aquifer Aquifer Gravel and Sand 1.0x10-9 1.0x10-7 25 35 Floral Formation Aquifers Aquifer Gravel and Sand 1.0x10-9 1.0x10-7 25 35 Sutherland Group Aquifers Aquifer Gravel and Sand 1.0x10-9 1.0x10-7 25 35 Empress Group Aquifer Aquifer Gravel and Sand 1.0x10-9 1.0x10-7 25 35 Compressibility of w ater at 25ºC is 4.8x10-10 m2/N * Domenico and Schw artz (1998) and Freeze and Cherry (1979) LL = Low er Limit UL = Upper Limit

For unconsolidated sediments, the compressibility of the soil is much greater than that of water so the specific storage is controlled by the compression of the pore skeleton. For rigid bedrock aquifers the opposite is true, with the specific storage controlled by the

M1890-1030109 Page 18 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 compressibility of the pore fluid. An increase in head or pore pressure results in a release of fluid from storage and a reduction in storage volume as the skeleton contracts. A reduction in head or pore pressure corresponds to an expansion of the storage volume as the skeleton dilates. The above behaviour is associated only with the elastic deformations.

3.6 Water Level Data Groundwater flows from areas of high hydraulic head to areas of low hydraulic head. Hydraulic head is a measurement of the energy state of a fluid (in this case groundwater) and is a function of potential energy (elevation head) and porewater pressure (pressure head). Velocity head is also a factor, but it is generally deemed negligible due to the low natural groundwater flow rates.

In central Saskatchewan, natural groundwater originates as infiltration of meteoric water, predominantly through sloughs, lakes, and other surface water bodies within groundwater recharge areas. Once below the water table, groundwater generally migrates vertically downward through the low permeability units (aquitards), and horizontally through the high permeability units (aquifers), until eventually discharging to the surface at a lower elevation relative to the infiltration point.

Water level information was obtained from WWDRs and the SWA observation well network. The water level provided in WWDRs is a single data point and therefore, cannot necessarily be considered “static” or representative of the natural system. This is particularly the case since many of the measurements were acquired by drillers during or following well installation and testing. As the number of water level readings increase for a single well, the reliability of the dataset also increases and can be used to identify long-term trends and events. Nevertheless, the point-water levels presented in the WWDRs were used to evaluate regional-scale lateral groundwater flow directions, while data from the SWA observation well network was used to provide long-term water level trends in the Saskatoon 73B area.

3.7 Groundwater and Surface Water Withdrawal Data Groundwater and surface water allocations were obtained from the SWA. Table 3.6 provides the licensed groundwater allocation at the time of writing this report. Table 3.6 was created by assigning WWDR IDs to the records within the Licensed Groundwater Database (as described in MDH, 2010a) and cross-referencing records to the stratigraphic interpretation completed as part of this study. The table indicates that the majority of the licensed groundwater use is from the Floral Formation and Empress Group aquifers.

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Table 3.6 – Groundwater allocations in the Saskatoon 73B area.

Formation (Strat. Symbol) Water Use # of Wells Allocation (dam3/y) Domestic 1 1 Irrigation 1 75 Surficial Stratified Deposits (Qssd) Municipal 33 700 Industrial 7 21 Domestic 1 1 Battleford Formation (Qb-s) Municipal 10 404 Domestic 4 6 Irrigation 1 285 Floral Formation (Qf-ms) Municipal 41 986 Industrial 4 199 Domestic 2 3 Irrigation 1 12 Floral Formation (Qf-ls) Municipal 9 343 Industrial 2 72 Warman Formation (Qw-s) Industrial 1 65 Municipal 6 461 Dundurn Formation (Qd-us) Industrial 3 8 Domestic 1 1 Mennon Formation (Qm-s) Municipal 1 14 Municipal 6 135 Empress Group (Qte) Industrial 1 2,400 Municipal 4 39 Judith River Formation (Kjr) Industrial 1 1 Municipal 9 100 Undifferentiated Industrial 7 7 Total 6,339 Notes: Strat. Symbol referenced to stratigraphic chart (Appendix A)

3.8 Groundwater Availability Groundwater availability is the amount of water available from the subsurface. The determination of groundwater availability is complicated by the fact that consideration must be given to often conflicting factors, including but not limited to: 1. The groundwater quality; 2. The cost to develop a groundwater resource; 3. The interconnectivity of an aquifer to the rest of the hydrogeological system (i.e. three-dimensional framework of hydrostratigraphic system), the hydrological system, and the ecosystem; 4. Socio-economics; and 5. The regulations and policies governing groundwater and surface water development and use (i.e. effective water and environmental management). Hydrogeologists need to study large-scale development projects in enough detail and over a sufficiently large area to allow the proponent and the regulatory bodies to make sound

M1890-1030109 Page 20 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 decisions on the sustainable development of a groundwater resource. Clearly defined and enforced regulations and policies are required to guide these projects to effectively manage sustainable water use in a potentially affected area. The best available way to estimate groundwater availability from a specific aquifer is completed by using 3D numerical analysis of a hydrogeological system that incorporates recharge, surface water features, topography, water withdrawals, and the influence of (and on) overlying and underlying hydrostratigraphic units. The thickness and areal limits of each unit need to be represented in sufficient detail to accurately simulate the groundwater system. This requires the availability of large borehole datasets often combined with geophysical methods.

Detailed determination of groundwater availability is beyond the scope of this study; however, available safe/sustainable yields from available groundwater investigation reports and, to lesser extent, recommended well yields/pumping rates from WWDRs provide an indication of how much water can be reasonably produced from an aquifer. Safe yields and well yields are often determined based on the results of short-term pumping test and provide information in the vicinity of the well and/or the observation well network. They should not be considered representative of the groundwater availability from the larger groundwater system. It is also noted that well yields provide a recommended pumping rate at the time of the test and do not necessarily provide an indication of the how long water can be produced at the stated rate or that the stated rate is sustainable. Safe yields and well yields do not typically address regional groundwater availability. This report provides only generalized, available assessments of water availability.

4.0 STRATIGRAPHY 4.1 Regional Geological Setting Successive marine transgression and regression in the Upper Cretaceous Period deposited a thick, complex sequence of marine silt and clay deposits across central Saskatchewan. The Upper Cretaceous aged Lea Park Formation shale constitutes the base of “freshwater” exploration associated with the shallow hydrostratigraphy in the study area; the Lea Park Formation (and its stratigraphic equivalent, the Pierre Formation) is a known marker horizon (i.e. it provides stratigraphic control) for most of southern Saskatchewan. The Lea Park Formation is composed of non-calcareous, grey, marine clay and silt (“shale”) found across the entire project area. There are no known receptors for contaminants below this formation in the study area.

Marine regression in the Upper Cretaceous Period resulted in the deposition of calcareous and non-calcareous stratified sands, silts, and clays over the Lea Park Formation shale. These stratified sands, silts, and clays are called the Judith River Formation. This unit is interpreted to exist in the southern portion of the study area and is found only as erosional remnants in the northern portion.

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The Bearpaw Formation is the uppermost “bedrock” unit encountered in the Saskatoon 73B area. It is composed of non-calcareous, grey, marine clay, silt, and sand (“shale”) which conformably overlies the Judith River Formation. The Bearpaw Formation is found predominantly in the south-southwestern part of the study area.

Prior to glaciation, the Saskatoon 73B area was mature and well integrated with a complex series of water courses and deep valleys. Erosion and subsequent alluvial and colluvial deposition of Tertiary-aged sediments filled these valleys. These sediments are generally comprised of preglacial quartz and chert sands and gravels, interbedded with organic rich silts and clays. Millions of years of deposition resulted in these preglacial deposits partially infilling these valleys.

The preglacial Tyner and Battleford Valleys form the dominant bedrock features in the Saskatoon 73B area. These valleys were cut into the bedrock surface primarily before and during the first glaciation (and to a lesser extent during subsequent glaciations) in the early Pliestocene Epoch. These valleys carried melt-water, depositing significant accumulations of clastic deposits within the lowland. The Tyner Valley runs from southwest to central Saskatchewan and the Battleford Valley runs from northwest to central Saskatchewan. These valleys have numerous tributaries, mesas, and plateaus and a complex hydrostratigraphy.

The stratified preglacial sediments deposited between the bedrock surface and the glacial sediments are formally called the Empress Group (Whitaker and Christiansen, 1972). These preglacial sediments sit unconformably on the bedrock surface and have been informally called the lower unit of the Empress Group. The sediments from the bedrock surface to the ground surface are collectively called “drift”. They are divided into preglacial and postglacial drift.

Over the past 2 million years, Saskatchewan has undergone at least eight periods (and possibly ten periods) of significant glacial advance. The final deglaciation occurred in the Pleistocene Epoch between approximately 17,000 and 10,000 years ago (Christiansen, 1979). Glaciation in the Pleistocene resulted in a complex arrangement of proglacial and glacial sediments interbedded with non-glacial stratified sediments (fluvial, deltaic, lacustrine, aeolian, etc.) deposited between glaciations and during interstadal deglaciation. Erosional valleys produced during interglacial periods commonly intersect preglacial valleys forming complex stratigraphic arrangements. The glaciofluvial, fluvial, alluvial and colluvial sediments that were deposited during preglacial and interglacial periods in the valleys were covered by tills during the final stages of glaciation, forming deep buried valley aquifer systems that are often flanked by more regionally extensive blanket aquifer systems. These systems are now buried with deposits from subsequent glacial and non-glacial periods, with limited indication of their presence at depth. They form the most significant freshwater aquifers in the province.

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The complex arrangement of glacial, glaciofluvial, and glaciolacustrine deposits within the study area are formally divided into two primary groups: 1) the Sutherland Group, and 2) the Saskatoon Group (Christiansen, 1992). Both the Saskatoon Group and the Sutherland Group are primarily comprised of unsorted till formed by glacial erosion and reworking of Precambrian igneous and metamorphic rocks, Paleozoic limestones, and Cretaceous marine shales during glacial advance. Significant intratill and intertill stratified deposits also comprise the Quaternary deposits.

The oldest till units of the Sutherland Group have a higher clay content compared to the overlying Saskatoon Group tills due to a higher percentage of marine shale being incorporated into the matrix of the till. Similarly, the Saskatoon Group tills have higher carbonate contents due to incorporation of more Paleozoic limestones and dolomites into the matrix. The lithological compilation, combined with carbonate content signatures, can be used to help identify each formation. The stratified deposits between these two groups, and between the individual till formations, represent the major aquifers across the study area.

Melting of the last glacier (between about 17,000 and 10,000 years ago) deposited a till plain characterized by a hummocky topography of kettles and eskers, covered with glacial and glaciofluvial/glaciolacustrine deposits and postglacial sediments (Surficial Stratified Deposits). These features form the surface topographic features in the area.

The complex stratigraphic arrangements of the Tertiary and Quaternary deposits were further complicated by extensive faulting due to either the dissolution of the deep evaporite deposits beneath the area and subsequent collapse of near surface sediments (Christiansen and Sauer, 2001), or by continental tectonic extension in the Cenozoic possibly combined with melting of gas hydrates during glacial retreat (Gendzwill and Stauffer, 2006). These depressions were infilled (generally with till) during subsequent glaciations, often resulting in discontinuous and hydraulically isolated accumulations of stratified deposits. Delineation of these collapse structures is important as they are often significant enough to displace aquifer units, resulting in lateral connectivity disruptions and significant aquifer boundary effects during water production.

The hydrostratigraphy of interest in the study area (in ascending order) is: 1. The Lea Park Formation; 2. The Judith River Formation; 3. The Bearpaw Formation; 4. The Empress Group; 5. The Sutherland Group: a. The Mennon Formation; b. The Dundurn Formation; and c. The Warman Formation; 6. The Saskatoon Group: a. The Floral Formation;

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b. The Battleford Formation; and c. The Surficial Stratified Deposits. A stratigraphic column of the Cretaceous and Quaternary units within the study area is provided in Appendix A. This provides the age, stratigraphy, lithology, and corresponding identification symbol used for potential stratigraphic units in southern Saskatchewan. A brief overview of each unit is provided in the following sections. In this report, depths and thicknesses are often related to a corresponding borehole using the WWDR ID (e.g. 220362 = borehole number (WWDR#) 220362). The relative locations of the borehole records and stratigraphic cross-sections are provided in Appendix B. The stratigraphic cross-sections are provided in Appendix C. The stratigraphic database of the boreholes in the hydrogeological study area is provided in Appendix D.

4.2 Bedrock Deposits In the Saskatoon 73B area, thick sequences of sand, silt, and clay of the Lea Park Formation (Lea Park Shale), the Judith River Formation, and the Bearpaw Formation (Bearpaw Shale) can form the bedrock subcropping. Figure E1 (Appendix E) provides a structure contour of the top of the Cretaceous deposits in the study area. This variability is attributed to faulting and pre-glacial and glacial erosion. Faulting should be considered when doing stratigraphic interpretations or investigations in southern Saskatchewan. The majority of faulting in southern Saskatchewan is due to salt dissolution collapse features. It is noted that “bedrock” in this geological setting is a misnomer, as the “bedrock” deposits are typically not fully cemented rocks. A brief overview of each unit is provided below.

The Lea Park Formation (western Saskatchewan) or the Pierre Formation (eastern Saskatchewan) is widely considered the base of “fresh water” exploration in southern part of the province due to brackish water in deeper horizons. Similarly, there are generally no perceived receptors for contamination below these horizons. As a result, these formations should be considered the base for drilling and instrumentation in relation to groundwater resource and/or environmental investigations in the study area.

4.2.1 The Lea Park Formation The Lea Park Formation (Klp) is generally comprised of non-calcareous, grey to dark grey, firm to hard, highly plastic, overconsolidated silt and clay. This formation is of marine origin and was deposited in the Western Interior Seaway during the Upper Cretaceous (McNeil and Caldwell, 1981). Concretionary and bentonitic rich beds are common in the Lea Park Formation. The bentonitic horizons can be used as structural marker beds for stratigraphic interpretations where delineated.

Figure E2 (Appendix E) shows a structure contour map of the top of the Lea Park Formation. The Lea Park Shale was encountered at depths ranging between 0.0 m at borehole 220362 (SHT Borden Bridge BH-15) and 292.6 m at 220589 (Midas #2). This unit has been encountered at elevations ranging from 220.4 masl (220589) to 574.6 masl (102283) across

M1890-1030109 Page 24 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 the study area. The deepest portions encountered in the study area correspond to locations where the Quaternary sediments are incised into the Upper Cretaceous sediments (e.g. 94230 (SRC Wanuskewin); Cross-section E-E’) and/or downward faulting of the bedrock surface has occurred. In the southern half of the 73B area, bedrock lows are often indicative of collapse due to dissolution of the underlying Prairie Evaporite Formation and subsequent downward faulting of the overlying stratigraphic sequences. The majority of the bedrock elevation variance in the northern half of the study area is due to erosion associated with the preglacial and interglacial valley deposits and associated tributaries.

The Ribstone Creek Member (Krc) of the Lea Park Formation is comprised of a complex arrangement of non-marine and marine stratified silts and sands. It has been further characterized as medium to very fine-grained sandstone, with buff weathering, friable to well indurated with calcite cement, cross-bedded in places, common carbonaceous fragments, and coal seams present in more westerly sections and interbedded mudstones in eastern sections (www.ir.gov.sk.ca). This member has been encountered in thicknesses up to 21.7 m, at 116777 (UofS Eagle No.29), in the study area. Cross-sections C-C’, D-D’, J-J’, K-K’, and L-L’ show locations where the Ribstone Creek is interpreted to be present.

4.2.2 The Judith River Formation The Judith River Formation (Kjr) is an eastward thinning sedimentary wedge found in north central United States, southern Alberta, and Saskatchewan. It is comprised predominantly of clays, silts, and sands deposited in a non-marine deltaic environment formed during a major regression of the marine environment in the Upper Cretaceous Epoch. This unit has isolated zones containing concretionary and carbonaceous horizons (McLean, 1971). The Judith River Formation can be up to hundreds of meters thick in Alberta. In the Saskatoon 73B area, the Judith River Formation has been encountered up to 75.9 m thick at 220400 (Eagle Hill #2), near Biggar. The Judith River Formation has been found at elevations ranging between 263.1 masl (220589) to 604.2 masl (86461) within the study area.

4.2.3 The Bearpaw Formation The Bearpaw Formation (Kb) consists predominantly of marine silts and clays deposited during the last major transgression and regression of the Western Interior Seaway. Dark grey clays, claystones, silty claystones, shales, silts and siltstones, with subordinate brownish grey silty sands, sands, and sandstones, numerous concretionary beds, and thin beds of bentonite characterize the Bearpaw Formation according to the Lexicon of Canadian Geology (http://cgkn1.cgkn.net).

Marine transgression and regression in the Upper Cretaceous Epoch deposited a complex sequence of interbedded sand/silt and silt/clay layers. These layers are identifiable on a regional scale and are formally identified as unique members of the Bearpaw Formation Within the Saskatoon 73B area, the Bearpaw Formation exists primarily as erosional remnants and where dissolution collapse has resulted in protection from erosion (see

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Appendix C). In the study area, this formation has been subdivided into five Members (Appendix A). In ascending order these are: 1. The Beechy Member (Kbby); 2. The Ardkenneth Member (Kba); 3. The Snakebite Member (Kbs); 4. The Cruikshank Member (Kbc); and 5. The Aquadell Member (Kbaq). The Bearpaw Formation has been encountered at depths ranging from 10.4 m (45302) to 148.0 m (202410). The formation thickness varies between 1.2 m (82478) and greater than 123.8 m (45302). Where present, the Bearpaw Formation has been found at elevations ranging from 388.6 masl (43758; Cross-section F-F’) to 625.8 masl (36174; Cross-sections A-A’ and J-J’) across the study area.

4.3 Preglacial Drift Deposits 4.3.1 The Empress Group The Empress Group (Whitaker and Christiansen, 1972) lies between the bedrock and the oldest (lowest) till. The Empress Group is composed of preglacial and proglacial stratified sediments. The Empress Group includes a wide variety of complexly bedded lithologies that were lain down as fluvial, lacustrine, and colluvial deposits on the bedrock surface prior to and during glaciation.

The Empress Group (QTe) is often divided into an upper (Qe) and lower (Te) unit. The lower unit is generally comprised of complexly stratified valley fill sediments which consist of quartzite and chert gravels, finer clastic deposits, and organic rich sediments. This unit is Tertiary in age (preglacial) and is often non-calcareous. The upper unit generally contains clastic sediments derived from igneous, metamorphic, and carbonate rocks that were deposited proglacially during the first glacial advance. The upper unit is often found within the bedrock valley tributaries and along the bedrock uplands. These deposits are generally calcareous due to some of the granular materials being derived from carbonate rocks along the Precambrian margin to the north and the Manitoba escarpment to the east. The presence of igneous and carbonate derived lithologies generally distinguish the upper unit from the lower (often non-calcareous) unit. The contact between the Empress Group and the overlying glacial deposits is an erosional unconformity.

The Empress Group has been encountered at depths varying ranging between 7.6 m (212247) and 224.3 m (35789; Cross-sections C-C’ and L-L’) across the Saskatoon 73B area. The Empress Group is variable in thickness, ranging from 0.3 m (119785) to 79.6 m (94230; Cross-section E-E’) where present. The thickest accumulations of Empress Group sediments can be expected in the thalwegs of the preglacial Tyner Valley and Battleford Valley. The contact between the Empress Group and the overlying glacial deposits is an erosional unconformity.

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4.4 Quaternary Drift Deposits The successive advance and retreat of continental glaciers deposited the geologic sequences that characterize the regional drift stratigraphy within the study area. The accumulations of sediments from the top of the Empress Group to the ground surface are collectively referred to as Quaternary drift. The Quaternary drift has been investigated intermittently and a number of papers have been published on the deposits (e.g. Christiansen, 1968a; Christiansen, 1968b; Christiansen, 1990; Christiansen, 1992; Christiansen and Sauer, 1994; etc.). The Quaternary deposits represent glacial and postglacial sediments and are separated into the Saskatoon Group and the Sutherland Group.

4.4.1 The Sutherland Group The Sutherland Group (Qsu) lies between the Empress Group and Saskatoon Group. Tills of the Sutherland Group can be distinguished from those of the Saskatoon Group based on the carbonate content of the tills, the stratigraphic relationship between the till and intertill deposits, Atterberg limits, preconsolidation pressures, jointing, staining, the presence of oxidized zones, their geophysical signatures, and their stratigraphic position. The Sutherland Group is separated into three formal formations, including (in ascending order): 1. The Mennon Formation (Qm); 2. The Dundurn Formation (Qd); and 3. The Warman Formation (Qw). Each of the formations of the Sutherland Group represent at least one distinct glacial period. The Dundurn Formation is comprised of at least two separate glaciations (three separate glacial periods may be represented within the Dundurn Formation). It is also thought that the Mennon Formation may represent two distinct glaciations. Separation of the formations of the Sutherland Group generally requires the use of laboratory testing data, in conjunction with visual descriptions, the mapping of intertill (not intratill) deposits, and paleo-oxidized horizons. Figure 4.1 provides a type log (210624, SHT Sutherland Overpass No.4) for the Saskatoon 73B area.

4.4.1.1 The Mennon Formation The Mennon Formation (Qm) is divided informally into three mappable units in the study area. In ascending order, these units are: 1. A lower till unit (Qm-lt) overlying Empress Group or bedrock deposits; 2. An intertill stratified deposit (Qm-s) at the break between the upper and lower till units; and 3. An upper till unit (Qm-ut). The Mennon Formation is discontinuous and sparse in the study area, and generally exists as erosional remnants along bedrock lows. In Saskatoon 73B area, the Mennon Formation

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011 has been encountered at depths ranging between 8.5 m (220309) and 220.7 m (35789; Cross-sections C-C’ and L-L’) where present. The Mennon Formation has been encountered in thicknesses up to 134.7 m (33184; Cross-sections A-A’ and I-I’). Tills of the Mennon Formation are generally comprised of a grey, unoxidized, weakly calcareous, low to medium plasticity, clayey silt till with varying accumulations of coarser and finer fractions. The Mennon Formation has a low carbonate content compared to the overlying till formations. The break between the Mennon Formation and the Dundurn Formation is also determined based on the presence of an intertill (not intratill) stratified unit (Qd-ls) and/or the presence of an oxidized contact.

4.4.1.2 The Dundurn Formation The Dundurn Formation (Qd) is divided informally into five mappable units in the study area. In ascending order, these units are: 1. A basal till unit (Qd-bt); 2. A lower stratified unit (Qd-ls); 3. A lower till unit (Qd-lt); 4. An intertill stratified deposit (Qd-us) at the break between the upper and lower till units; and 5. An upper till unit (Qd-ut). Differentiation of these units is based on carbonate content, the presence of paleo-oxidized horizons and/or intertill stratified deposits (Qw-s, Qd-us, and Qd-ls). The carbonate content of the upper unit of the Dundurn Formation (Qd-ut) is higher than that of the Warman or Mennon Formations, but typically lower than that of the Floral Formation. The carbonate content often decreases across the lower unit of the Dundurn Formation (Qd-lt), as shown in Figure 4.1. It should be noted that differentiation of the Mennon Formation, Dundurn Formation, and Warman Formation is difficult without carbonate contents and/or the presence of intertill stratified deposits.

Tills of the Dundurn Formation are generally comprised of grey, unoxidized, calcareous, silt and clay till with varying accumulations of coarser and finer fractions. It is found over a large part of the study area, but is still considered discontinuous due to post-depositional erosion. The Dundurn Formation has been interpreted to exist in thicknesses up to 131.7 m (35789; Cross-sections C-C’ and L-L’) in the study area. This formation has been encountered at depths ranging from 0.0 m to 135.9 m (39564; Cross-section C-C’). The upper till unit of the Dundurn Formation is readily identifiable from the overlying Warman Formation based on carbonate content.

4.4.1.3 The Warman Formation The Warman Formation (Qw) lies between the Dundurn Formation and the Floral Formation where present. The Warman Formation is differentiated from the overlying and underlying formations based on the presence of a paleo-oxidized contact, carbonate contents,

M1890-1030109 Page 29 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 geophysical signatures, Atterberg limits, and the presence of mappable stratified deposits (Qf-ls and Qw-s, respectively). It is noted that mappable stratified deposits are verified intertill units (not intratill deposits). The Warman Formation has relatively low carbonate contents and high clay contents, making it readily identifiable from the overlying Saskatoon Group tills and the underlying upper till unit of the Dundurn Formation.

Tills of the Warman Formation are generally comprised of grey, medium to highly plastic, calcareous, silty clay till. The Warman Formation has been encountered in thicknesses up to 63.4 m (108787) in the Saskatoon 73B area. The depth to this unit ranges from 0.0 m to 116.7 m (31586; Cross-section F-F’), where encountered across the study area.

4.4.2 The Saskatoon Group The Saskatoon Group (Qsk) was first proposed by Christiansen (1968a) as the portion of drift lying between the Sutherland Group and the topographic surface. The Saskatoon Group is differentiated from the underlying Sutherland Group on the basis of carbonate content, resistivity signatures, lithologic characteristics, Atterberg limits, and preconsolidation pressures. The Saskatoon Group tills have higher carbonate contents and resistivity signatures, and are generally coarser in lithology, with respect to the underlying Sutherland Group tills (i.e. the Sutherland Group tills generally have significantly higher clay contents). The higher clay content of the Sutherland Group tills is also reflected by Atterberg limits (when available) with a higher plasticity index relative to Saskatoon Group tills.

The Saskatoon Group is formally separated into three formal formations, including (in ascending order): 1. The Floral Formation (Qf); 2. The Battleford Formation (Qb); and 3. The Surficial Stratified Deposits (Qssd).

4.4.2.1 The Floral Formation In the study area, the Floral Formation (Qf) is divided informally into five units. In ascending order, these units are: 1. A basal till unit (Qf-bt); 2. An lower intertill stratified deposit (Qf-ls); 3. A lower till unit (Qf-lt); 4. An middle intertill stratified deposit (Qf-ms); and 5. An upper till unit (Qf-ut). Delineation of these units is based on the presence of paleo-oxidized horizons and/or intertill stratified deposits (Qb-s, Qf-ms, and Qf-ls), and, to a lesser extent, carbonate contents. Tills of the Floral Formation are predominantly firm to hard, low to high plasticity, silt till with varying accumulations of coarser and finer fractions. The Floral Formation has been

M1890-1030109 Page 30 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 encountered at depths of 0.0 m to 97.5 m (45654; Cross-section F-F’) in the Saskatoon 73B area, and in thicknesses up to 112.8 m (220555).

The upper till unit of the Floral Formation is identified by iron and manganese stained fractures and strong oxidization (where present). The firm to hard consistency and fractured nature of this upper till unit make it readily identifiable from the Battleford Formation till, which is generally much softer than the Floral Formation. The Floral Formation tills have a preconsolidation pressure of 1,800 ± 200 kPa, whereas till of the Battleford Formation has a preconsolidation pressure of 400-750 kPa (Sauer et al., 1993). The contact between the Floral Formation and the overlying Battleford Formation is non-conformable.

4.4.2.2 The Battleford Formation The Battleford Formation (Qb) was first described by Christiansen (1968b) and is typically composed of soft, massive, oxidized till, and is the youngest formation of the Saskatoon Group. The Battleford Formation till was deposited during the last glaciation period and has not been overridden by any subsequent glaciers. As a result, it is readily separated from the underlying Floral Formation based on its soft consistency. In the study area, the Battleford Formation has been encountered in thicknesses up to 114.0 m (220561), immediately south of Saskatoon.

4.4.2.3 The Surficial Stratified Deposits The Surficial Stratified Deposits (Qssd) are the top unit of the Saskatoon Group. These postglacial sediments include fluvial, lacustrine, aeolian, and topsoil deposits. The Surficial Stratified Deposits are divided into Haultain and alluvium. Alluvium is found in river valleys, whereas clays, silts, sands, and gravels of the Haultain unit are found at the ground surface anywhere else. Accumulations of these sediments occur over much of the Saskatoon 73B area. Up to 96.9 m (219509; immediately north of Clavet) of Surficial Stratified Deposits are interpreted to be encountered in this area.

5.0 HYDROGEOLOGY Deposits of silts, sands, gravels, and cobbles form relatively high hydraulic conductivity units that form the paths of least resistance for groundwater flow and solute transport. These units are called aquifers. An aquifer is defined as saturated geologic unit that is permeable enough to transmit significant quantities of water under ordinary hydraulic gradients, or as the term is commonly used in the water-well industry: an aquifer is a saturated geologic unit that is permeable enough to yield economic quantities of water to wells (e.g. Freeze and Cherry, 1979; Kruseman and de Ridder, 1990). Aquifers can be part of a geological formation, the entire formation or group of formations. Conversely, silt and clay rich deposits form low hydraulic conductivity units that impede groundwater flow and solute transport. An aquitard is a saturated geologic unit which is permeable enough to transmit water in significant quantities when viewed over large areas and long periods, but does not yield economic quantities of water to wells (Kruseman and de Ridder, 1990). These units are

M1890-1030109 Page 31 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 called aquitards and generally have hydraulic conductivities of less than 1x10-7 m/s. The spatial arrangement of aquifers and aquitards in three-dimensions form the hydrostratigraphy of a site. When combined with the physical characteristics of the hydrostratigraphic units, an overall view of the hydrogeology can be determined.

Gravel, sand, silt, and/or clay predominantly comprise the Surficial Stratified Deposits (Qssd), the intertill stratified deposits (Qb-s, Qf-ms, Qf-ls, Qw-s, Qd-us, Qd-ls, and Qm-s), the Empress Group (QTe) sediments, and the Upper Cretaceous sand/silt stratified units (Kbc, Kba, Kjr, and Krc); the lithology of these stratified deposits can vary significantly over short distances and be aquifers or aquitards depending on lithology, hydraulic connectivity, potential well yields, etc. For simplicity, these mappable stratified deposits are described as aquifers in Section 5 of this report. The interpretations provided should not be used for decisions relating to a development or well installation without verification (i.e. confirmatory drilling). The compiled maps and cross-sections should only be used to provide the framework for the area and to make large-scale general decisions to guide site specific investigations. Although none of these horizons are comprised of laterally continuous gravels and sands, the complexities of the mappable stratified deposits do not preclude the potential of finding lithologies capable of supplying small quantities of water. The actual amount of water available will be based on the site specific hydraulic properties of the sediments, and the thickness and lateral continuity of higher permeability sediments.

Bedrock silts, sands, gravels, and preglacial valley fill sediments form major “freshwater” aquifers across Saskatchewan. Figure 5.1 shows the approximate location of the major shallow bedrock and buried valley aquifers across Saskatchewan. The preglacial Battleford and Tyner Valleys are the major bedrock buried valley aquifer systems in the area.

In addition to the major buried valley aquifers incised into the marine shales, the overlying Quaternary aged stratum contains both blanket and channel deposits of sand and gravel that were deposited by retreating and/or advancing glaciers. These deposits are found between the major till units and are called intertill stratified deposits. These intertill stratified deposits can form broad, laterally extensive aquifers and/or small channel aquifers, depending on their depositional setting and subsequent erosion. Although intratill deposits are abundant, they generally form only isolated, discontinuous pockets, and are therefore not significant with respect to groundwater sourcing.

In the Saskatoon 73B area, there are nine major mappable horizons, above the Lea Park Formation, that may contain aquifer sediments, these are as follows (in ascending order): 1. The Judith River Formation Stratified Deposits (Kjr, Judith River Aquifer); 2. The Ardkenneth Member Stratified Deposits (Kba, Ardkenneth Aquifer); 3. The Cruikshank Member Stratified Despoits (Kbc, Cruikshank Aquifer); 4. The Empress Group Stratified Deposits (QTe, Empress Group Aquifer); 5. The Mennon Formation Stratified Deposits (Qm-s, Mennon Aquifer); 6. The Lower Dundurn Formation Stratified Deposits (Qd-ls, Lower Dundurn Aquifer);

M1890-1030109 Page 32 ALBERTA MANITOBA SASKATCHEWAN ³

MANVILLE AQUIFER

CUMBERLAND AQUIFER

BATTLEFORD VALLEY AQUIFER

"WYNYARD FORMATION" AQUIFER JUDITH RIVER AQUIFER

EMPRESS BEDROCK GROUP TERTIARY AQUIFER AQUIFER TURNER VALLEY AQUIFER AQUIFER FORMED BY BEARPAW SAND

SWIFT CURRENT VALLEY AQUIFER HATFEILD VALLEY AQUIFER

JUDITH RIVER AQUIFER VALLE EASTEND-RAVENSCRAG AN Y A UIFER d Q x EV

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LEGEND 4 2 - 4 2 SASKATOON 73B MAPSHEET AREA CUMBERLAND AQUIFER EMPRESS GROUP AQUIFER JUDITH RIVER AQUIFER - 0 9 8

BEARPAW FORMATION AQUIFER QUATERNARY AND/OR TERTIARY AQUIFER ESTEVAN VALLEY AQUIFER MANNVILLE GROUP AQUIFER 1 M \ D

TERTIARY AQUIFER EASTEND-RAVENSCRAG AQUIFER HATFIELD VALLEY AQUIFER NO MAJOR PREGLACIAL AQUIFER PRESENT X M _ B 3 7

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MAJOR PREGLACIAL AQUIFER 1 M _

BOUNDARIES OF SASKATCHEWAN A

SCALE 1:3,500,000 DATE W S \ SUPERVISED BY G. POTTER, M.Sc., P.Eng. 24-FEB-11 PRODUCED BY PROJECT M1890-1030009 FIG. No. 5.1 A W S \ DRAWING : DRAWN BY S. LONG, GIS Cert. 24-FEB-11 L

M1890-24-24 : h t

APPROVED BY A. KARVONEN, M.Sc., P.Eng., P.Geo. 24-FEB-11 a P Hydrogeological Mapping of the Saskatoon 73B Area April 2011

7. The Upper Dundurn Formation Stratified Deposits (Qd-us, Upper Dundurn Aquifer); 8. The Warman Formation Stratified Deposits (Qw-s, Warman Aquifer); 9. The Lower Floral Formation Stratified Deposits (Qf-ls, Lower Floral Aquifer); 10. The Middle Floral Formation Stratified Deposits (Qf-ms, Upper Floral Aquifer); 11. The Battleford Formation Stratified Deposits (Qb-s, Battleford Aquifer); and 12. The Surficial Stratified Deposits (Qssd, Surficial Aquifer).

5.1 The Judith River Aquifer The Judith River Formation is comprised of Upper Cretaceous clays, silts, and sands deposited in a non-marine shoreline environment typical of deltaic deposits (McLean, 1971). The Judith River Formation was encountered predominantly in the southern half of the Saskatoon 73B area, as this unit subcrops north of Saskatoon (Figure F1; Appendix F). The sediments of Judith River Formation form a major aquifer in Saskatchewan, referred to as the Judith River Aquifer. This aquifer is not commonly accessed for use as a “fresh water” resource due to its waters being highly mineralized and the presence of shallower aquifers. The Judith River Aquifer is laterally discontinuous (Appendix C) in the Saskatoon 73B area due to extensive faulting, such that only low volume users could potentially use it as a resource. Furthermore, there tends to be shallower aquifers in the study area that can be more readily accessed.

5.1.1 Hydraulic Properties There are limited available hydraulic conductivity measurements for the Judith River Aquifer in the Saskatoon 73B area, although third party measurements are known to exist. Kewen and Schneider (1979) reported hydraulic conductivities ranging from 1.9x10-6 m/s to 1.7x10-5 m/s, with an average of 7.1x10-6 m/s. These values can be considered representative of bulk hydraulic conductivities in this unit. Based on the experience of MDH, values of less than 1.9 x10-6 m/s can be found locally.

5.1.2 Groundwater Flow Generally, the Judith River Aquifer is recharged by the infiltration of meteoric water and the inflow of connate water from the overlying and underlying shales. The hydraulic head distribution within the Judith River Aquifer is expected to be complex in the Saskatoon 73B area due to extensive faulting due to salt dissolution collapse, although there are a limited number of wells to confirm this. Lateral groundwater flow within this aquifer is predominantly toward the North Saskatchewan River where in outcrops (Cross-sections A-A’, B-B’, and C-C’). Lateral groundwater flow is also interpreted to be toward the South Saskatchewan River. Groundwater flow in this aquifer is also strongly influenced by flow (and water development) within the deep Empress Group Aquifers (e.g. Tyner Valley Aquifer), where incised into the Judith River Aquifer.

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5.1.3 Groundwater Availability There were no third party reports available to provide an idea of safe or sustainable yield from the Judith River Aquifer in the study area. Sixty-five driller’s records show a range in recommended pumping rates from 20 m3/d to 196 m3/d, with an average of 59 m3/d. While this says nothing of the groundwater availability, it does provide some indication on expected well yields from the Judith River Aquifer. Given the discontinuous nature and depth of the Judith River Formation the sustainable yield from this aquifer is expected to be low for the Saskatoon 73B area. This aquifer is not recommended as a groundwater source if flow rates of >65 m3/d are required. It is noted that multiple wells may be required to obtain sufficient quantities of water and will depend on the local hydraulic properties.

The allocated water withdrawal from licensed wells installed in the Judith River Aquifer is approximately 40 dam3/y in the Saskatoon 73B area. Of this allocation, <7 m3/d is used. This is predominantly for municipal use in Elstow and Arlee.

5.1.4 Groundwater Quality A Piper Plot of available tested groundwater samples from the Judith River Aquifer in the study area is provided in Figure 5.2. Water from the Judith River Aquifer is predominantly characterized as sodium-sulfate type water. However, the Piper Plot illustrates that sampled water from this aquifer ranges from sodium- and/or calcium-bicarbonate to sodium-chloride type water.

In the majority of samples, the Canadian Council of Ministers of the Environment (CCME) drinking water objective for sodium and sulfate is exceeded (200 mg/L and 500 mg/L, respectively). The objective for chloride (250 mg/L) is also exceeded in a number of samples. The TDS concentration of groundwater from the Judith River Aquifer ranged from 950 mg/L (Rutherford 1489) to 8,260 mg/L (Rutherford 1366). In the study area, water from this unit is generally not suitable for human consumption, irrigation, or livestock watering without treatment.

5.1.5 Groundwater Vulnerability Figure G1 (Appendix G) shows the vulnerability of the Judith River Aquifer to contamination from the surface in the Saskatoon 73B area. The aquifer vulnerability index (AVI) is predominantly low to very low, except where this formation is encountered near surface or where thick overlying aquifer units are present (e.g. Cross-section A-A’). Since the AVI map is based on calculations at borehole locations, the AVI index should be very high at all locations where any of the mappable aquifer units are interpreted to outcrop.

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011

5.2 The Ardkenneth Aquifer The Ardkenneth Member of the Bearpaw Formation is composed predominantly of unoxidized, generally silty, very fine- to fine-grained sand with lesser amounts of interbedded silts and clays. The Ardkenneth Aquifer is limited in areal extent and discontinuous in the study area (Figure F2; Appendix F). The Ardkenneth Aquifer has been encountered at depths ranging between 46.9 m (220578) and 158.5 m (9517) in the Saskatoon 73B area. This unit is generally about 15 m to 25 m thick, where encountered in the study area.

5.2.1 Hydraulic Properties Hydraulic properties were not available for the Ardkenneth Aquifer in the study area. A hydraulic conductivity range of 1x10-6 m/s to 1x10-4 m/s has been estimated for this unit. Maathuis and Simpson (2007) estimated the hydraulic conductivity of Bearpaw Formation sands members to be 1.2x10-5 m/s to 5.8x10-5 m/s.

5.2.2 Groundwater Flow There is limited information on water levels in this hydrostratigraphic unit within the Saskatoon 73B area. Based on limited information, groundwater flow in the eastern portion of the Ardkenneth Aquifer is toward the South Saskatchewan River. While there are no wells installed in the western portion of the Ardkenneth Aquifer, groundwater flow is likely in a northerly direction toward the North Saskatchewan River. Groundwater flow in this aquifer will be complex due to structure introduced by salt dissolution collapse.

5.2.3 Groundwater Availability There were no third party reports available to provide an idea of safe or sustainable yield from the Ardkenneth Aquifer in the study area. Only two water wells are interpreted to be installed in this unit. Pumping tests on these two wells appear to have been unsuccessful. Given the seemingly poor pumping test results, coupled with the discontinuous nature and depth of this sand unit, it is not a recommended target for water supply in the Saskatoon 73B area.

5.2.4 Groundwater Quality The two piezometers installed in the Ardkenneth Aquifer yielded a sodium-sulfate type water (Figure 5.3), exceeding the CCME drinking water objective for both sodium and sulfate. This water is similar to the water sampled from the Judith River Aquifer. The aesthetic objective for chloride was also exceeded in water sampled from 112762. Generally, this water is not considered suitable for human consumption, irrigation, or livestock watering without treatment.

5.2.5 Groundwater Vulnerability Figure G2 (Appendix G) shows the vulnerability of the Ardkenneth Aquifer to contamination from the surface in the Saskatoon 73B area. The aquifer vulnerability index (AV) is predominantly low to very low, with moderate ratings in several localized areas.

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011

5.3 The Cruikshank Aquifer The Cruikshank Member of the Bearpaw Formation is composed predominantly of unoxidized, silty, very fine- to fine-grained sand with lesser amounts of interbedded silts and clays. The Cruikshank Aquifer is limited in areal extent and discontinuous in the study area, as shown in Figure F3 (Appendix F). It is only present where preserved due to the down faulting associated with salt dissolution collapse structures.

The Cruikshank Aquifer has been encountered at depths ranging between 51.0 m (33003; Cross-section I-I’) and 100.6 m (211199) in the Saskatoon 73B area. The thickness of this unit ranged from 9.1 m (220593) to 22.6 m (211200) where encountered. Hydraulic properties were not available for the Cruikshank Aquifer in the study area, but are expected to be similar to the Ardkenneth Aquifer.

5.3.1 Groundwater Flow In the Saskatoon 73B area, there are no available water levels in the Cruikshank Member but lateral groundwater flow will likely be influenced by the groundwater flow within overlying and underlying mappable stratified deposits.

5.3.2 Groundwater Availability In the Saskatoon 73B area, the Cruikshank Aquifer is limited in areal extent and should not be targeted for water supply.

5.3.3 Groundwater Quality Groundwater quality data was not available for the Cruikshank Member since there were no wells interpreted to be installed in this aquifer.

5.3.4 Groundwater Vulnerability Figure G3 (Appendix G) shows the vulnerability of the Cruikshank Aquifer to contamination from the surface in the Saskatoon 73B area. The aquifer vulnerability index (AV) is predominantly low to very low, with a localized moderate rating south of Saskatoon.

5.4 The Empress Group Aquifer Sands and gravels of the Empress Group infill a portion of the pre-glacial Tyner Valley and Battleford Valley, which form two of the most significant and prolific aquifers in the Saskatoon 73B area. The stratified deposits in these valleys comprise two of the largest “fresh water” aquifer systems in the province, extending from inside Alberta and pinching out in the vicinity of Saskatoon (Figure 5.1).

Valley fill aquifer systems in Saskatchewan, such as the Tyner or Battleford Valley Aquifers, often contain several hydrostratigraphic units which can result in hydraulic connection of several aquifer horizons. Figure F4 (Appendix F) shows the lateral extent and thickness of the Empress Group Aquifer in the study area, as well as the approximate location of the

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Tyner Valley, the Battleford Valley, and the Meacham Aquifers. Most of the cross-sections show interpreted and/or potential interconnectivity between the Empress Group sediments and younger mappable intertill stratified deposits, especially in the vicinity of the Tyner Valley Aquifer (Cross-sections D-D’, E-E’ F-F’, I-I’, and J-J’), the Battleford Valley Aquifer (Cross- sections A-A’, B-B’, and K-K’), and the Meacham Aquifer (Cross-sections G-G’ and I-I’).

5.4.1 Hydraulic Properties The hydraulic properties of the Empress Group Aquifer have been explored in many investigations across Saskatchewan, as it is readily exploited for industrial, municipal, and domestic water use. Hydraulic conductivities of the Empress Group Aquifer generally range between 1x10-5 m/s to 5x10-4 m/s. Jaques (1989) reported a hydraulic conductivity and a transmissivity of 1x10-5 m/s and 164 m2/d, respectively. Transmissivities from the Tyner Valley Aquifer determined at observation wells during the constant-rate pumping test(s) for TransGas ranged from 4,954 m2/d to 10,627 m2/d (Beckie Hydrogeologists (1990) Ltd. (BHL), 2003), with storage coefficients between 3-5x10-4. Transmissivities between 200 m2/d to 2,500 m2/d, with storage coefficients around 2x10-4, are typical according to Maathuis and Schreiner (1982).

5.4.2 Groundwater Flow Groundwater within the Empress Group Aquifer is recharged by downward flow through overlying strata and lateral flow from interconnected aquifers, including, but not limited to, the Judith River Aquifer. Vertical flow between the Empress Group Aquifer and the overlying and underlying formations is significantly less than lateral groundwater flow within the unit. Vertical recharge to the unit is slow due to the thick, low permeability confining units (overlying till and underlying marine shales). The majority of recharge to the aquifer occurs at slow rates through the overlying glacial drift and through lateral inflow from bedrock units. The lateral boundaries of the aquifer are formed by the Upper Cretaceous marine deposits (in which it is incised) and the overlying till.

Lateral groundwater flow within the Tyner Valley Aquifer is in a northerly direction, toward the North Saskatchewan River, where it discharges. Lateral groundwater flow in the Battleford Valley Aquifer is also toward the North Saskatchewan River, where it also discharges. Groundwater flow in the Meacham Aquifer is likely east-southeasterly in direction toward the main channel of the Hatfield Valley Aquifer System. The Hatfield Valley Aquifer crosses the entire province in a northwest to southeast direction (Figure 5.1). The main channel of the Hatfield Valley Aquifer is located east and north of the Saskatoon 73B area. This valley is at least 30 km wide, with a thickness that often exceeds 100 m along the thalweg. The Meacham Aquifer is characterized as a blanket aquifer that sits on the shoulder of the Hatfield Valley Aquifer. Blanket sand and gravel deposits along the shoulder of the Hatfield Valley Aquifer are common in the province.

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The SWA has three observation wells installed in the Empress Group Aquifer: • SWA Duck Lake 2 (34715), located on the shoulder of the Hatfield Valley Aquifer in the northeast quadrant of the study area, • SWA Vanscoy (32338), completed in the Tyner Valley Aquifer near Vanscoy, and • SWA Blucher No.3 (112761), completed in the Meacham Aquifer on the shoulder of the Hatfield Valley Aquifer in the southeast quadrant of the study area. Figure 5.4 and Figure 5.5 show the hydrographs from wells 34715 and 112761. They both show <1 m variation in hydraulic head over the monitored periods because there are no large users of this aquifer in the vicinity of these wells. Water levels measured at these locations show natural seasonal and temporal variability.

479.8

479.7

479.6

479.5

479.4

479.3

Hydraulic Head (masl) 479.2

479.1

479.0

478.9

478.8 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.4 – Hydrograph SWA Duck Lake 2 (34715). Water levels at 32338 (Figure 5.6) show similar seasonal and annual changes, until 2004, when TransGas started groundwater production at rates of approximately 2,600 m3/d to 6,500 m3/d for cavern development from a hydraulically impeded portion of the Tyner Valley Aquifer. High volume water production by TransGas in 2004 caused significant drawdowns in the Tyner Valley aquifer and in the overlying Tessier Aquifer (comprised of the Upper and Lower Floral Aquifers). The initial groundwater investigation (BHL, 2003) and subsequent review (Maathuis, 2005; Maathuis et al., 2007) stress the importance of detailed groundwater sourcing studies for high capacity groundwater usage and long-term monitoring to ensure groundwater resources are developed in a sustainable manner with respect to all potentially affected aquifers (i.e. overlying and underlying aquifers) and stakeholders.

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520.0

519.8

519.6

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Hydraulic Head (masl) 518.8

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518.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.5 – Hydrograph for SWA Blucher No.3 (112761).

510.0

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500.0 Hydraulic Head (masl)

498.0

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492.0 1-Jan-60 1-Jan-65 2-Jan-70 3-Jan-75 4-Jan-80 4-Jan-85 5-Jan-90 6-Jan-95 7-Jan-00 7-Jan-05 8-Jan-10 9-Jan-15 Date (mmm-yy) Figure 5.6 – Hydrograph for SWA Vanscoy (32338).

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5.4.3 Groundwater Availability In the Saskatoon 73B area, licensed groundwater water production and allocation from the Empress Group sediments was 92 dam3/y and 2,535 dam3/y, respectively, with the majority being used by TransGas. Aberdeen and the community of Neuhorst use approximately 9% of the produced groundwater for tank load facilities while Cathedral Bluffs Ltd., Denholm, Maymont, and Speers use approximately 9% for municipal supply. The recommended pumping rate from the 89 WWDRs ranged from 20 m3/d to 393 m3/d for wells installed in the Empress Group. Since the Empress Group often discharges to the river valleys, the available drawdown is typically small toward the North and South Saskatchewan Rivers. The depth to water from WWDRs ranged from flowing artesian to 88.4 m.

The net sustainable water production capacity from the Tyner Valley Aquifer System is estimated to be 128,767 m3/d or 47,000 dam3/y (Meneley, 1972). The peak groundwater production rate (6,532 m3/d) required by TransGas for cavern development appears to have exceeded the safe yield for this hydraulically impeded portion of the Tyner Valley Aquifer. It is noted that this high volume production was for short-term use and sustainable/safe yield is based on long-term water production. Jaques (1989) estimated a safe yield of 5,095 m3/d from a well completed in Empress Group sediments in the Battleford Valley Aquifer. An extensive pumping test, coupled with numerical modelling, is typically required to quantify groundwater availability, as it is highly dependent on aquifer discontinuities and the three- dimensional configuration of the entire groundwater system. The Empress Group Aquifer is likely the only aquifer in the study area that is capable of producing large volumes of water (i.e. >20 m3/d) for industrial use.

5.4.4 Water Quality Groundwater in deep buried valley aquifers can be variable, and in most cases, is highly mineralized, hard, and sulfate rich. Groundwater entering a deep aquifer from the overlying glacial deposits has undergone considerable chemical evolution and some of the groundwater may represent water trapped during deposition of the tills. A Piper Plot of the groundwater samples obtained from the Empress Group Aquifer is provided in Figure 5.7.

The water is primarily characterized as sodium-sulfate type water (76 percent of samples), similar to the water sampled from the Judith River Aquifer. This indicates that the water is generally derived from the overlying till sequences and connate water from the Upper Cretaceous sands, silts, and shales in which it is incised. This is typical of the Empress Group Aquifer in most areas of Saskatchewan.

Groundwater samples from the Empress Group in the Saskatoon 73B area indicate that it is generally not potable without treatment. In the majority of samples, the CCME aesthetic objectives for sodium and sulfate are exceeded. The aesthetic objective for chloride is also exceeded in a number of samples. The TDS concentration ranges between 876 mg/L (36203) and 5,470 mg/L (9649), with an approximate average of 2,500 mg/L, making the

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011 aquifer a poor source of water for irrigation due to soil salinization concerns. However, water from the Empress Group Aquifer is often used for domestic purposes (when treated) and as a direct water supply for livestock.

5.4.5 Groundwater Vulnerability Figure G4 (Appendix G) shows the vulnerability of the Empress Group Aquifer to contamination from the surface in the Saskatoon 73B area. The aquifer vulnerability index (AV) is low to very low. However, the Empress Group Aquifer is expected to be susceptible to contamination where it outcrops into the river valleys (e.g. Cross-section A-A’).

5.5 The Mennon Aquifer The Mennon Aquifer generally overlies the lower till unit of the Mennon Formation (where it is not eroded). This unit can also sit directly on the bedrock surface. A complex arrangement of gravel, sand, silt, and clay comprises this aquifer. The Mennon Aquifer is discontinuous in the Saskatoon 73B area and is most extensive in the northwest quadrant; Figure F5 (Appendix F) shows the interpreted areal limits of the Mennon Aquifer. It has been encountered in thicknesses between 0.6 m and 36.6 m (35971; Cross-section B-B’) and depths of 15 m (220284) to 147.5 m (33184, Cross-sections A-A’ and I-I’), in the study area.

5.5.1 Hydraulic Properties Hydraulic properties were not available for the Mennon Aquifer in the Saskatoon 73B area. A hydraulic conductivity range of 1x10-6 m/s to 5x10-4 m/s can be expected for the sands and gravels. Significantly lower hydraulic conductivities can be expected for the silt and clay units within this aquifer.

5.5.2 Groundwater Flow There are a limited number of wells and water levels available from the Mennon Aquifer in the mapsheet. In the western have of the study area, groundwater flow is toward the North Saskatchewan River.

5.5.3 Groundwater Availability Licensed groundwater allocation and production from the Mennon Aquifer is low. Maymont has a well installed in this unit that produces approximately 1.4 dam3/y and has an allocation of 13.6 dam3/y. Approximately 1 dam3/y is allocated and used by one licensed domestic user near Denholm. The Mennon Aquifer is likely hydraulically connected to the Empress Group Aquifer and is part of the Battleford Valley Aquifer System in the study area. A large-scale pumping test with observation wells installed in multiple-aquifer horizons, coupled with 3D groundwater flow modelling, would likely be required to better determine groundwater availability in this system.

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5.5.4 Groundwater Quality A Piper Plot of the groundwater obtained from the Mennon Aquifer is provided in Figure 5.8. The Piper Plot illustrates that the water type is quite varied with the most common types being calcium-bicarbonate, sodium-sulfate, and calcium-sulfate type waters. The concentrations of sodium and sulphate often exceed respective CCME aesthetic objectives in the sampled groundwater. The CCME objective for chloride was exceeded in one of the samples (55440) from the Mennon Aquifer. Water that is high in sodium, calcium, and sulfate is indicative of water derived from the overlying glacial till sequences, coupled with some mixing of connate water from the Upper Cretaceous marine shales. This water type is similar to that of the Empress Group Aquifer.

5.5.5 Groundwater Vulnerability Figure G5 (Appendix G) shows the vulnerability of the Mennon Aquifer to contamination from the surface in the Saskatoon 73B area. The aquifer vulnerability index (AVI) is low to very low, with the exception of a small moderate area in the vicinity of the Petrofka Bridge. The moderate AVI near Petrofka Bridge is due to the interpretation of Mennon Aquifer near surface in a borehole(s) in the vicinity of the bridge.

5.6 The Lower Dundurn Aquifer The Lower Dundurn Aquifer is generally comprised of a complex arrangement of gravel, sand, silt, and clay. Figure F6 (Appendix F) shows the interpreted areal limits of this aquifer. The Lower Dundurn Aquifer is discontinuous in the Saskatoon 73B area. It is interpreted to be encountered in thicknesses up to 50.6 m (35789; Cross-sections C-C’ and L-L’) and depths of 0.0 m (73947) to 150.9 m (34573, Cross-section G-G’). The Lower Dundurn Aquifer may be hydraulically connected to Empress Group sediments at several locations in the study area. Cross-sections E-E’, F-F’, and I-I’ show where this aquifer is likely part of the Tyner Valley Aquifer System. Cross-section G-G’ shows where the Lower Dundurn Aquifer is likely associated with the Meacham Aquifer System. Pumping tests with instrumentation in multiple aquifer units would be required to confirm hydraulic connectivity in these stacked aquifer systems.

5.6.1 Hydraulic Properties Hydraulic properties were not available for the Lower Dundurn Aquifer in the Saskatoon 73B area. A hydraulic conductivity range of 1x10-6 m/s to 5x10-4 m/s can be expected for the sands and gravels. Significantly lower hydraulic conductivities can be expected for the silt and clay units within this aquifer.

5.6.2 Groundwater Flow The lateral groundwater flow direction in the Lower Dundurn Aquifer could only be determined for the northwest quadrant of the mapsheet due to the discontinuous and isolated nature of this aquifer in the other quadrants. Southerly to westerly groundwater flow

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011 directions were observed north of the North Saskatchewan River, toward this river. The groundwater flow directions in this unit will be similar to that of the Upper Dundurn Aquifer over the rest of the mapsheet.

5.6.3 Groundwater Availability Third party well reports and associated safe or sustainable yields were unavailable for the Lower Dundurn Aquifer in the Saskatoon 73B area. Thirty driller’s records show a range in recommended pumping rates from 7 m3/d to 72 m3/d, with an average of 131 m3/d. While this says nothing of the groundwater availability, it does provide some indication on expected well yields from this aquifer. The sustainable yield from the Lower Dundurn Aquifer is expected to be low given the discontinuous nature and variable lithology of this unit. There are no licensed allocations for this aquifer in the study area.

5.6.4 Groundwater Quality A Piper Plot of the groundwater sampled from the Lower Dundurn Aquifer is provided in Figure 5.9. This water is predominantly characterized as a sodium-sulfate type water. The CCME objective for these two analytes is exceeded in most of the samples. Without treatment, this water is generally not suitable for human consumption, irrigation, or for livestock water supply.

5.6.5 Groundwater Vulnerability Figure G6 (Appendix G) shows the vulnerability of the Lower Dundurn Aquifer to contamination from the surface in the Saskatoon 73B area. Due to this unit’s depth, the aquifer vulnerability index (AVI) is generally low to very low. There are several small sections rated as moderate, with a point very high reading at borehole 73947, where the Lower Dundurn Aquifer is interpreted to outcrop.

5.7 The Upper Dundurn Aquifer The Upper Dundurn Aquifer is generally comprised of a complex arrangement gravels, sands, silts, and clays. Figure F7 (Appendix F) shows the interpreted thickness and areal extent of the Upper Dundurn Aquifer in the study area. The thickness of this unit is variable as a result of both post-depositional erosion and/or non-deposition. The Upper Dundurn Aquifer was encountered in thicknesses up to 67.7 m (64512) in the Saskatoon 73B area. The interpreted depth of this unit ranges from 0.0 m (204051, 204052) to 147.5 m (34573; Cross-section G-G’).

Similar to the Lower Dundurn and Mennon Aquifers, potential hydraulically connectivity with the Empress Group sediments exists in the study area. Cross-sections D-D’, F-F’, I-I’, and J-J’ show where the Upper Dundurn Aquifer may be part of the Tyner Valley Aquifer System. Cross-section G-G’ shows where this aquifer may be part of the Meacham Aquifer System.

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011

5.7.1 Hydraulic Properties Hydraulic properties of the Upper Dundurn Aquifer have been assessed in the Saskatoon 73B area. The transmissivity determined during the constant-rate pumping test of Well No.3A for Biggar ranged from 265 m2/d to 338 m2/d (J.D.Mollard and Associates, 1976). The hydraulic conductivity of the Upper Dundurn Aquifer will typically range between 1x10-6 m/s and 1x10-3 m/s. Significantly lower hydraulic conductivities can be expected for wells completed in silts or clays within this aquifer.

5.7.2 Groundwater Flow Groundwater flow in the Upper Dundurn Aquifer is generally toward the nearest river valley in the Saskatoon 73B area. This is based on 209 point water level readings from WWDRs in the area. The Upper Dundurn Aquifer is recharged by the downward migration of meteoric water through the overlying sediments.

The SWA has two observation wells installed in the Upper Dundurn Aquifer: • SWA Warman #1 and #2 (32049 and 32050), between Dalmeny and Warman; (Cross-section J-J’) and • SWA Hague (34663), south of Rosthern (Cross-section F-F’). Figure 5.10 and Figure 5.11 show the hydrographs from wells 32049 and 32050. These observation wells show <1.4 m variation in hydraulic head over the last 35 years due to natural seasonal and temporal variability.

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Hydraulic Head (masl) 451.9

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451.5 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.10 – Hydrograph for SWA Warman #1 (32049).

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453.0

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Hydraulic Head (masl) 451.8

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451.2

451.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.11 – Hydrograph for SWA Warmam #2 (32050). Figure 5.12 shows the hydrograph for well 34663. Water levels at this location show a gradual decrease of approximately 2 m between the early 1970s and 2005.

5.7.3 Groundwater Availability In the Saskatoon 73B area, licensed groundwater production and allocation from the Upper Dundurn Aquifer was approximately 39 dam3/y and 469 dam3/y, respectively, with the majority (97%) being used by the Town of Biggar (Biggar). Less than 2% of the licensed allocation is for industrial agriculture and the rest is used for recreational and tankload facilities. The recommended pumping rate from WWDRs ranged from <7 m3/d to 1,964 m3/d, with an average of 98 m3/d for wells installed in this aquifer. The 1,964 m3/d rate can likely be regarded as an upper limit to sustainable groundwater production from this aquifer in the area. An extensive pumping test, coupled with numerical modelling, is typically required to quantify groundwater availability, as it is highly dependent on aquifer discontinuities and the three-dimensional configuration of the entire groundwater system.

5.7.4 Groundwater Quality Groundwater within large intertill blanket aquifers (like the Upper Dundurn Aquifer) has typically undergone considerable chemical evolution, similar to the deeper buried channel aquifers such as the Empress Group Aquifer. A Piper Plot of chemistry data from available groundwater samples obtained from the Upper Dundurn Aquifer is provided in Figure 5.13.

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466.0

465.5

465.0

464.5

464.0 Hydraulic Head (masl)

463.5

463.0

462.5 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.12 – Hydrograph for SWA Haque (34663).

The groundwater is characterized as sodium-bicarbonate to calcium-magnesium sulfate type water.

Groundwater from the Upper Dundurn Aquifer is generally not potable (without treatment) and is very hard and sulfate rich. It typically exceeds several CCME drinking water quality objectives, including (but not limited) to TDS, sodium, and sulfate. The TDS concentration ranges from 797 mg/L (48808) to 2,870 mg/L (34663) in sampled groundwater. The objectives for sodium and sulfate are exceeded in the majority of samples, while the objective for chloride is exceeded in about 25% of the samples.

5.7.5 Groundwater Vulnerability Figure G7 (Appendix G) shows the vulnerability of the Upper Dundurn Aquifer to contamination from the surface in the Saskatoon 73B area. The aquifer vulnerability index is generally low to very low due to this unit’s depth. However, there are several areas rated moderate to high, with a point very high reading at boreholes 204051 and 204052, where the Upper Dundurn Aquifer is interpreted to outcrop.

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011

5.8 The Warman Aquifer The Warman Aquifer is comprised of a complex arrangement of gravels, sands, silts, and clays, typically at the contact between the Warman Formation and the underlying Dundurn Formation. Figure F8 (Appendix F) shows the interpreted areal extent and thickness of the Warman Aquifer. This aquifer is discontinuous across the study area and generally occurs as isolated intertill stratified deposits. This aquifer has been encountered in thicknesses up to 39.0 m (219599) in the Saskatoon 73B area and at an average depth of 48.5 m.

5.8.1 Hydraulic Properties In the Saskatoon 73B area, hydraulic conductivity was not available for the Warman Aquifer but can be expected to range between 1x10-6 m/s to 5x10-4 m/s in the sand and gravel units. The hydraulic conductivity will be significantly less in silt and clay units within this aquifer.

5.8.2 Groundwater Flow Lateral groundwater flow is toward the river valleys within the Warman Aquifer.

5.8.3 Groundwater Availability There were no third party reports available to provide an idea of safe or sustainable yield from the Warman Aquifer in the study area. Licensed groundwater allocation and production from the Warman Aquifer is 65 dam3/y and 5 dam3/y, respectively, from a single intensive livestock operation. Eighteen driller’s records show a range in recommended pumping rates from 7 m3/d to 196 m3/d, with an average of 98 m3/d. While this says nothing of the groundwater availability, it does provide some indication on expected well yields from this aquifer. Given the discontinuous nature and depth of this unit, the sustainable yield from this aquifer is expected to be low for the Saskatoon 73B area.

5.8.4 Groundwater Quality A Piper Plot of the groundwater sample obtained from wells 13407 and 70701, installed in the Warman Aquifer, is provided in Figure 5.14. The groundwater is characterized as calcium-sulfate type water. The sulphate concentration exceeds the CCME objective in both samples. The water sampled from 13407 also exceeds the objective for sodium. The chloride concentration is very low in both samples (31 mg/L and 3 mg/L, respectively). This water chemistry may not be representative of the Warman Aquifer in the study area, since water chemistry data was only available for two locations.

5.8.5 Groundwater Vulnerability Figure G8 (Appendix G) shows the vulnerability of the Warman Aquifer to contamination from the surface in the Saskatoon 73B area. The AVI ranges from very low to moderate across the study area. The AVI is predominately low due to the depth of this aquifer in the study area.

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011

5.9 The Lower Floral Aquifer Interbedded stratified deposits often occur at the contact between the Sutherland Group and the Saskatoon Group. This unit has been informally called the Lower Floral Aquifer. The Lower Floral Aquifer is interpreted to be discontinuous in the study area, as shown in Figure F9 (Appendix F). The Lower Floral Aquifer has been encountered in thicknesses up to 53.0 m (31585; Cross-section I-I’) and at depths between 2.4 m (219507; Cross-section F- F’) and 104.2 m (39564; Cross-section C-C’), in the Saskatoon 73B area.

The Lower Floral Aquifer may be hydraulically connected to the Upper Floral Aquifer at several locations within the study area. These hydrostratigraphic units form important aquifers in the Saskatoon area formally named: 1. the Fielding Aquifer, 2. the Dalmeny Aquifer, 3. the Tessier Aquifer, and 4. the Forestry Farm Aquifer (Figure F9). It is also noted that sediments interpreted as belonging to the Upper Floral Aquifer may be part of the Lower Floral Aquifer, since these two units are lithologically similar. Where directly connected it is very difficult, if not impossible, to differentiate these units.

5.9.1 Hydraulic Properties Hydraulic properties were obtained from available reports and were found to be within the expected range. Groundwater investigations in the area (JD.Mollard and Associates, 1967; Golder and Associates, 1985; Gillies et al., 1986) estimated the transmissivity and storativity to range between 35 m2/d to 197 m2/d and 3x10-4 to 8x10-4, respectively. The hydraulic conductivity of the this aquifer is expected to be within the 1x10-6 m/s to 1x10-3 m/s range.

5.9.2 Groundwater Flow Infiltration of meteoric water through the Saskatoon Group sediments recharges the Lower Floral Aquifer. Lateral groundwater flow in the Lower Floral Aquifer is generally toward the nearest river valleys where these units discharge as springs along the valley walls. The groundwater flow in the Fielding Aquifer is toward the North Saskatchewan River, while groundwater flow in the Forestry Farm Aquifer is toward the South Saskatchewan River on the west side of the Strawberry Hills and southeasterly in direction on the east side of the Strawberry Hills. Groundwater flow in the Dalmeny Aquifer is toward both the North and the South Saskatchewan Rivers, with the groundwater flow divide interpreted to occur along between the Langham and Martensville. Groundwater flow in the Tessier Aquifer is generally east to northeasterly in direction. Figure 5.15 shows a hydrograph for SWA Blucher No.4 (31403), installed in the Forestry Farm Aquifer. This hydrograph shows <1 m change, suggesting natural variability in the Lower Floral Aquifer at this location.

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520.0

519.8

519.6

519.4

519.2

519.0

Hydraulic Head (masl) 518.8

518.6

518.4

518.2

518.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.15 – Hydrograph for SWA Blucher No.4 (31403).

5.9.3 Groundwater Availability In the Saskatoon 73B area, licensed groundwater water production and allocation from the Lower Floral Aquifer was 41 dam3/y and 431 dam3/y, respectively, with the majority (80%) being allocated to municipally by Blaine Lake, Marcelin, Waldheim, and Mayfair. Intensive livestock operations are allocated approximately 17% and the rest is licensed to domestic and irrigation uses. The recommended pumping rate from the 109 WWDRs ranged from 13 m3/d to 393 m3/d for wells installed in the Lower Floral Aquifer.

Sustainable well yields of 196-327 m3/d (J.D.Mollard and Associates, 1967) to 2,180 m3/d (Roper Environmental Engineering Inc., 1992) in the lower unit of the Dalmeny Aquifer and the Fielding Aquifer, respectively. This can likely be regarded as an upper limit for sustainable yield for the Lower Floral Aquifer within the Saskatoon 73B area. It is noted that higher individual well yields could be possible but water requirements at these rates would likely require extensive testing, multi-well arrays, and could have large scale impacts.

The impact on overlying aquifer units due to pumping of the Lower Floral Aquifer should be evaluated at pumping rates greater than 196 m3/d; this is required to determine impact on other water users in the area and assist in the determination of safe yields. An extensive pumping test, coupled with numerical modelling, would be required to quantify groundwater availability at any given location in the mapsheet, as it is highly dependent on aquifer

M1890-1030109 Page 57 Hydrogeological Mapping of the Saskatoon 73B Area April 2011 discontinuities, the three-dimensional configuration of the groundwater flow system, and the rate of groundwater production from wells and well fields.

5.9.4 Groundwater Quality A Piper Plot of the groundwater chemistry for the Lower Floral Aquifer is provided in Figure 5.16. The groundwater is predominantly characterized as calcium-sulfate, calcium- magnesium-sulfate, or calcium bicarbonate type water, typical of water derived from glacial deposits. The TDS concentration ranged in sampled groundwater ranged from 1,170 mg/L (112842) to 3,100 mg/L (31402). The TDS and sulfate concentrations generally exceed the respective CCME drinking water quality objectives.

5.9.5 Groundwater Vulnerability The Lower Floral Aquifer has been impacted by several anthropogenic developments at surface in Saskatchewan and is a concern for potential contaminant migration. Figure G9 (Appendix G) shows the vulnerability of this aquifer unit to contaminants from the surface. The AVI is predominantly moderate, but ranges from low to very high in the Saskatoon 73B area.

5.10 The Upper Floral Aquifer Interbedded stratified deposits occur at the contact between the upper and lower till units of the Floral Formation (i.e. the Riddell Member). This unit has been informally called the Upper Floral Aquifer. The Upper Floral Aquifer is often complexly stratified and can include significant till horizons due to interstadal glacial retreat and advance (e.g. 106188; Cross- section A-A’). This is a common occurrence within the Floral Formation aquifers across the province.

The Upper Floral Aquifer may be hydraulically connected to the Lower Floral Aquifer at several locations in the study area. These units form important aquifers in the Saskatoon 73B area formally named: 1. the Fielding Aquifer, 2. the Dalmeny Aquifer, 3. the Tessier Aquifer, and 4. the Forestry Farm Aquifer (Figure F9). It is also noted that sediments interpreted as belonging to the Upper Floral Aquifer may be part of the Lower Floral Aquifer, since these two units are lithologically similar.

5.10.1 Hydraulic Properties The Upper Floral Aquifer has been explored in many investigations, as it is readily exploited for industrial, municipal, and domestic water use in the Saskatoon 73B area; however, publically available pumping test results on this hydrostratigraphic unit are limited. The

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011 minimum, mean, and maximum hydraulic properties of the Dalmeny Aquifer determined by MDH (2010b) near Langham was: 1. Transmissivity – 130 m2/d, 432 m2/d, and 708 m2/d, respectively; 2. Storativity – 3.9x10-4, 7.3x10-4, and 1.6x10-3, respectively; and 3. Hydraulic conductivity – 6.2x10-5 m/s, 2.1x10-4 m/s, and 3.7x10-4 m/s, respectively. BHL (2004) estimate transmissivity and storativity of 217-602 m2/d and 8.7x10-4, respectively, for the Dalmeny Aquifer near Langham. Roper (1992) estimated the following hydraulic properties for the Fielding Aquifer, near Radisson: 1. Transmissivity – 360 m2/d to 720 m2/d; 2. Storativity – 1.8x10-4; and 3. Hydraulic conductivity – 2.0x10-4 m/s to 3.5x10-4 m/s. Similar to the other aquifers, the hydraulic conductivity of the Upper Floral Aquifer is expected to range between 1x10-6 m/s and 1x10-3 m/s.

5.10.2 Groundwater Flow Infiltration of meteoric water through upper Saskatoon Group sediments (Surficial Stratified Deposits, Battleford Formation, and Upper Floral Formation) recharges the Upper Floral Aquifer; this is predominantly through depression focused recharge. In the study area, the vertical component of groundwater flow is generally downward to and from this aquifer toward respective underlying formations.

Vertically downward groundwater flow to the underlying Sutherland and Empress Group aquifers could amount to a loss of water, from the Dalmeny Aquifer to these aquifers, of 10-20% of the total recharge to the Dalmeny Aquifer (Fortin et al., 1989). BHL (2004) estimated a recharge rate of 3.5 mm/y (about 1% of the annual precipitation) to the Dalmeny Aquifer. Fortin et al. (1989) estimated a rate of recharge of 5 mm/y (about 1.4% of the annual precipitation), accounting for all sources of recharge and discharge at the time. Recharge to the Upper Floral Aquifer is expected to generally range between 1 mm/y and 10 mm/y, depending on location.

Lateral groundwater flow in the Upper Floral Aquifer is effectively the same as that of the Lower Floral Aquifer, typically toward the nearest river valleys. The groundwater flow in the Fielding Aquifer is toward the North Saskatchewan River, while groundwater flow in the Forestry Farm Aquifer is toward the South Saskatchewan River on the west side of the Strawberry Hills and southeasterly in direction on the east side of the Strawberry Hills. Groundwater flow in the Dalmeny Aquifer is toward both the North and the South Saskatchewan Rivers, with the groundwater flow divide interpreted to occur between the Langham and Martensville. Groundwater flow in the Tessier Aquifer is generally east to northeasterly in direction.

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Figure 5.17 shows a hydrograph for SWA Dalmeny (32128) installed in the Dalmeny Aquifer. The hydrograph shows over 6 m of variation in its 40+ year history. This may be indicative of a gradual decline in water levels due to pumping and subsequent recovery. Figure 5.18, Figure 5.19, and Figure 5.20 show hydrographs from wells installed in the Forestry Farm Aquifer. While decreasing water levels were not observed, a similar increase was observed between 2005 and 2008, suggesting natural causes (i.e. more infiltration).

511.0

510.0

509.0

508.0

507.0 Hydraulic Head (masl) 506.0

505.0

504.0

503.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.17 – Hydrograph for SWA Dalmeny (32183). 5.10.3 Groundwater Availability The Upper Floral Aquifer is a water source used mainly for municipal purposes in the Saskatoon 73B area. The 986 dam3/y of groundwater presently allocated for municipal use from this aquifer is being used for: 1. Community and institutional purposes in the vicinity of Maymont and Hepburn; 2. Recreational purposes in the vicinity of Hafford; 3. Tankload and rural distribution in the rural municipalities of Aberdeen, Biggar, Blaine Lake, Perdue, and Rosthern; and 4. Urban distribution for Hafford, Hague, Aberdeen, Asquith, Biggar, Duck Lake, Langham, Raddison, and Ruddell. Municipal use accounts for 67% of the licensed allocation from the Upper Floral Aquifer in the study area. Approximately 19% and 14% of the licensed allocation is for irrigation near

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502.0

501.5

501.0

500.5

500.0

499.5 Hydraulic Head (masl)

499.0

498.5

498.0

497.5 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.18 – Hydrograph for SWA Saskatoon (31803).

496.0

495.8

495.6

495.4

495.2

495.0

Hydraulic Head (masl) 494.8

494.6

494.4

494.2

494.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.19 – Hydrograph from Silverspring MW21.

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492.6

492.5

492.4

492.3

492.2

492.1

Hydraulic Head (masl) 492.0

491.9

491.8

491.7

491.6 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.20 – Hydrograph from Silverspring MW10.

Dalmeny and several industrial operations, respectively. It is noted that about half of the allocated water from the Upper Floral Aquifer was used.

Water production from an aquifer that exceeds recharge to the aquifer is generally undesirable. Groundwater BHL (2004) estimates 299 dam3/y of infiltration to the Dalmeny Aquifer per year assuming 1% of the precipitation infiltrates and recharges the aquifer. This can likely be considered the lower bound for expected recharge to this aquifer. Fortin et al. (1989) estimated 1,200 dam3/y to the northern half of the Dalmeny Aquifer alone, based on discharge rates along the North Saskatchewan River. The dynamic nature of the Dalmeny Aquifer hydrograph (Figure 5.17) is not typical of deeper intertill aquifers and suggests that the Dalmeny Aquifer may be recharged by rapid infiltration of waters from surface.

Roper (1992) estimated the theoretical 20-year yield from the Fielding Aquifer to be 880 dam3/y, while MDH (2010b) estimated a theoretical 20-year yield of 792 m3/d for a well installed in the Dalmeny Aquifer east of Langham. The maximum recommended pumping rate from WWDRs was 393 m3/d. It is noted that safe yields and well yields do not typically address regional groundwater availability. Inflow and outflows from complexly configured hydrostratigraphic units generally require 3D numerical groundwater flow modelling to estimate the effects of large and small scale pumping on the entire groundwater flow system. Groundwater availability from the Upper Floral Aquifer has not been assessed with respect to the entire hydrogeological system.

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5.10.4 Groundwater Quality A Piper Plot of the groundwater sampled from the Upper Floral Aquifer is provided in Figure 5.21 and Figure 5.22. The Piper Plot illustrates that the groundwater chemistry from the Upper Floral Aquifer is very similar to that of the Lower Floral Aquifer. The water from the Upper Floral Aquifer is characterized as a calcium-sulfate, calcium-bicarbonate, sodium- sulfate, and calcium-magnesium-sulfate type water.

Water in the Upper Floral Aquifer is rich in sulfate, with the CCME objective being exceeded in 68% of samples. Sulfate rich groundwater is typical for waters that have migrated through glacial deposits, whereas bicarbonate type water is typically caused by the dissolution of carbonates and dolomites by carbonic acid (H2CO3) in the shallow surface. Carbonic acid is formed when infiltrating rainwater reacts with CO2 generated in the soil. Infiltrating rainwater has migrated through and reacted with glacial deposits to form the chemical make-up of the groundwater within the Upper Floral Aquifer.

The TDS concentration ranges from 674 mg/L to 3,140 mg/L in sampled groundwater from this aquifer. The CCME objective for sodium is exceeded in 27% of the samples. In all but one of the samples, the chloride concentration is below the CCME objective of 250 mg/L. The chloride concentration is below 50 mg/L in the majority of samples (76%).

5.10.5 Groundwater Vulnerability Figure G10 (Appendix G) shows the vulnerability of Upper Floral Aquifer to contamination from a surficial source in the Saskatoon 73B area. The AVI is predominantly high due to the proximity of these stratified deposits to the surface. There are some very high to moderate rated patches in the study area.

5.11 The Battleford Aquifer Stratified sediments at the contact between the Battleford and Floral Formation are informally named the Battleford Aquifer in this report. Figure F11 (Appendix F) shows the thickness and the areal limits of this unit in the Saskatoon 73B area. This aquifer has been interpreted to occur at depths of 0.0 m to 42.0 m (219558), but on average has been encountered at depths of approximately 3.3 m. The encountered thickness of the Battleford Aquifer is up to 59.1 m (13450) in the study area.

5.11.1 Hydraulic Properties Hydraulic properties for the Battleford Aquifer in the Saskatoon 73B area were obtained from available groundwater investigation reports in the vicinity of Biggar. The transmissivity and storativity was estimated to range from 298 m2/d to 1,477 m2/d and 2.5x10-4 to 5.8x10-3, respectively. The hydraulic conductivity of the Battleford Aquifer is expected to be within the typical range for an aquifer (1x10-3 m/s to 1x10-3 m/s). Pumping test results and analysis were not available for other water wells installed in the study area.

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5.11.2 Groundwater Flow Lateral groundwater flow within the Battleford Aquifer will be strongly topographically focused. The groundwater flow pattern within this unit will be generally focused towards local sloughs and depressions. This aquifer is generally recharged by infiltrating meteoric water. Figure 5.23 shows the hydrograph for SWA Agrium 43 (219583), interpreted to be installed in the Battleford Aquifer near Rice Lake. The fluctuation in water levels appears to be natural at this location. Cross-section C-C’ shows that the Battleford Aquifer may be hydraulically connected to Upper Floral Aquifer at this location or that intertill stratified deposit that 219583 could be interpreted as Upper Floral Aquifer sediments.

5.11.3 Groundwater Availability The Battleford Aquifer is generally not used for water supply due to its discontinuous nature and shallow depth. In the study area, licensed groundwater water production and allocation from the Battleford Aquifer was 44 dam3/y and 404 dam3/y, respectively, with the majority (91%) being allocated to Biggar. Biggar has several wells installed in a thick sequence of stratified deposits with a safe yield of 1,964 m3/d. The safe yields for portions of the Battleford Aquifer over the rest of the Saskatoon 73B area are expected to be significantly less. The recommended pumping rate for the five wells interpreted to be installed in other portions of the Battleford Aquifer (i.e. not the portion of the aquifer used for Biggar’s water supply) ranged from 13 m3/d to 98 m3/d. The Battleford Aquifer is typically shallow, relatively thin, and discontinuous, and therefore should not be expected to supply much water.

498.4

498.2

498.0

497.8

497.6 Hydraulic Head (masl)

497.4

497.2

497.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.23 – Hydrograph for SWA Agrium 43 (219583).

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5.11.4 Groundwater Quality A Piper Plot of the analyzed groundwater from the Battleford Aquifer (available for the study area) is provided in Figure 5.24. Water from this aquifer is characterized as calcium- magnesium-bicarbonate to calcium-magnesium-sulfate type water, typical of water in recharge to discharge zones, respectively. While there was no TDS data available for piezometers installed in the Battleford Aquifer, the water can be expected to range between relatively fresh to highly mineralized.

5.11.5 Groundwater Vulnerability Figure G11 (Appendix G) shows the vulnerability of the Battleford Aquifer in the Saskatoon 73B area. The AVI is predominantly high to very high for this mappable stratified unit. This aquifer is susceptible to contamination from the surface.

5.12 The Surficial Aquifer A complex arrangement of stratified post-glacial sediments comprise the Surficial Stratified Deposits. These deposits have been encountered in thicknesses of over 96.9 m (219509) in the Saskatoon 73B area, but on average are 11.4 m thick. Figure F12 (Appendix F) shows the interpreted lateral extent and thickness of the Surficial Stratified Deposits. The depth, thickness, and extent of individual gravels, sands, silts, and clays are highly variable and the hydraulic connectivity between these units is highly complex. Due to complexity of these deposits, a simplified interpretation is presented herein as they may form a relatively continuous “aquifer” in some areas. These stratified sediments are informally named the Surficial Aquifer in the study area.

5.12.1 Hydraulic Properties Many towns and RMs use the Surficial Stratified Deposits for water supply. Hydraulic properties for surficial sand aquifers in the Saskatoon 73B area are summarized from available groundwater investigations, as follows: 1. Transmissivity – 130 m2/d to 4,000 m2/d; 2. Storativity – 0.003 to 0.20 3. Hydraulic conductivity – 2.6x10-4 m/s to 2.2x10-3 m/s. 5.12.2 Groundwater Flow Groundwater flow within the Surficial Aquifer will be strongly topographically focused. The groundwater flow pattern within this unit will be generally focused towards sloughs and depressions on a local and toward the river valleys on a regional scale. The infiltration of meteoric water predominantly recharges this aquifer is the study area.

Figure 5.25 shows the hydrograph for SWA Duck Lake No. 1 (34714) (adjacent to 34718 on Cross-sections F-F’ and L-L’), installed in the Surficial Stratified Deposits near Duck Lake. Figure 5.26 shows the hydrograph for SWA Goodale Farm 9 (43769) (immediately north of

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Hydrogeological Mapping of the Saskatoon 73B Area April 2011

500.5

500.0

499.5

Hydraulic Head (masl) 499.0

498.5

498.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.25 – Hydrograph for SWA Duck Lake No. 1 (34714).

508.0

507.5

507.0

506.5

506.0

505.5

Hydraulic Head (masl) 505.0

504.5

504.0

503.5

503.0 Jan-60 Jan-65 Jan-70 Jan-75 Jan-80 Jan-85 Jan-90 Jan-95 Jan-00 Jan-05 Jan-10 Jan-15 Date (mmm-yy) Figure 5.26 – Hydrograph for SWA Goodale Farm 9 (43769).

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43758 on Cross-section F-F’), installed in the Surficial Stratified Deposits southeast of Saskatoon.

5.12.3 Groundwater Availability The sustainable yield from a surficial sand and /or gravel unit will depend largely on the thickness, areal extent, recharge rate, and available drawdown. The sustainable aquifer yield for Rosthern’s water supply decreased from 365 dam3/y to 200-250 dam3/y based on increasing knowledge of the groundwater system with time. The surficial aquifer used by Duck Lake has an estimated average sustainable aquifer capacity of 95 dam3/y. An adaptive monitoring plan is typically recommended to ensure water production from a near surface groundwater resource is sustainable.

In the Saskatoon 73B area, licensed groundwater water production and allocation from the surficial aquifers was 75 dam3/y and 732 dam3/y, respectively, with the majority being used for municipal purposes. The recommended pumping rate from the 39 WWDRs ranged from 0 m3/d to 262 m3/d for wells installed in the Surficial Stratified Deposits. While it is possible to obtain water from surficial sands and gravels, the sustainable groundwater production is largely a function of recharge, areal extent, and complexity of the deposits.

5.12.4 Water Chemistry Groundwater chemistry in shallow subsurface can be quite variable depending on residence time in the ground. In recharge zones, the groundwater will be relatively fresh due to the limited residence time of the groundwater in the near surface deposits. Bicarbonate type water is caused by the dissolution of carbonates and dolomites by carbonic acid (H2CO3).

Carbonic acid is formed when infiltrating rainwater reacts with CO2 generated in the soil. Higher TDS concentration groundwater can be expected in local shallow discharge zones and can be highly mineralized. Evaporative concentration of minerals in the near surface deposits occurs in the vicinity of groundwater discharge zones. This evaporative concentration results in higher analyte concentrations and high TDS concentrations.

A Piper Plot of the groundwater chemistry for the Surficial Stratified Deposits is provided in Figure 5.27 and is indicative of both short and long residence time within the groundwater flow system. The Piper Plot shows the typical progression of groundwater from “fresh” recharge area water to highly-mineralized discharge area water. TDS concentrations measured in the Surficial Stratified Deposits ranged from 278 mg/L (123127) to 1,320 mg/L (220503). Most of the water sampled was relatively “fresh” and characterized as calcium- magnesium-bicarbonate type water. However, some of the sampled water was very hard and sulfate rich, typical of a discharge zone.

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5.12.5 Groundwater Vulnerability Figure G12 (Appendix G) shows the vulnerability of the Saskatoon 73B area to contaminants at surface. Surficial Stratified Deposits have a very high AVI since they are at surface. Figure G12 shows that the majority of the Saskatoon 73B area is susceptible to contamination from a surface source. The vulnerability of surficial aquifers will be dependent on the lithologies and thickness of any aquitard sediments near surface within the Surficial Stratified Deposits.

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6.0 CLOSURE The hydrogeological mapping of the Saskatoon 73B NTS Mapsheet was completed as authorized by the Saskatchewan Watershed Authority. This report was prepared for the Saskatchewan Watershed Authority in accordance to generally accepted geo-environmental engineering practice, no other warranty, expressed or implied is made.

We trust that this report meets your needs. Please contact the undersigned if you have any question or concerns, or if we can be of further assistance.

Respectfully submitted,

MDH Engineered Solutions Corp. Association of Professional Engineers and Geoscientists of Saskatchewan Certificate of Authorization Number 662

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7.0 DISCLAIMER The information presented in this document was compiled exclusively for the Saskatchewan Watershed Authority. MDH Engineered Solutions Corp. does not accept any responsibility for the use of this report for any purpose other than intended or to any third party for the whole or part of the contents and exercise no duty of care in relation to this report to any third party.

The compiled information is subject to error and is only intended to provide the stratigraphic framework for the area and to make large-scale general decisions to guide site specific investigations. As a result of this uncertainty, the interpretations provided based on this data should not be used for decisions relating to a development or well installation without verification (i.e. confirmatory drilling). All interpretations should be completed by a professional geoscientist. Any alternative use, including that by a third party, or any reliance on, or decisions made based on this document, are the responsibility of the alternative user or third party. MDH Engineered Solutions Corp. accepts no responsibility for damages, if any, suffered by any third party as a result of decisions made or actions based on this report.

MDH Engineered Solutions Corp. has exercised reasonable skill, care and diligence to assess the information acquired during the preparation of this report, but makes no guarantees or warranties as to the accuracy or completeness of this information. This report is based upon and limited by circumstances and conditions acknowledged herein, and upon conditions encountered at the time of the writing of this report.

Any questions concerning the information or its interpretation should be directed to MDH Engineered Solutions Corp.

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8.0 REFERENCES Acton, D.F., Padbury, G.A., and C.T. Stushnoff, 1998. The Ecoregions of Saskatchewan. Hignell Printing Ltd., Winnipeg. Agriculture and Agri-Food Canada (AAFC), 2002. Gross evaporation for the 30-year period 1971-2000 in the Canadian Prairies by Prairie Farm Rehabilitation Administration (PFRA). Hydrology report #143. Beckie Hydrogeologists Ltd., 1980. Report on Well Installation Program for the Town of Biggar. Prepared for the Prairie Farm Rehabilitation Administration. May 1980. Beckie Hydrogeologists Ltd., 1987. Report on Test Drilling and Test Well Installation Program for the Town of Rosthern, Saskatchewan 1986-87. Prepared for the Prairie Farm Rehabilitation Administration. January 1987. Beckie Hydrogeologists Ltd., 1988a. Town of Biggar – 1987 Contract No.1 Drilling and Well Installation of Well PW5-87. February 1988. Beckie Hydrogeologists Ltd., 1988b. Report on Well Installation Program for the Town of Rosthern. Prepared for the Prairie Farm Rehabilitation Administration. December 1988. Beckie Hydrogeologists Ltd., 2000. Town of Rosthern Wellfield Expansion 1999. Prepared for the Town of Rosthern. February 2000. Beckie Hydrogeologists (1990) Ltd., 2003. TransGas Ltd. Saskatoon West Water Source Development Project Proposed Natural Gas Storage Caverns. October 2003. Beckie Hydrogeologists (1990) Ltd., 2004. Town of Langham 2003 Groundwater Exploration Program. February 2004. Beckie Hydrogeologists Ltd., 2008. Town of Duke Lake Groundwater Exploration and Water Well(s) Development Project Consulting Services Agreement 2007A-00736. April 2008. Caldwell, W.G.E., 1968. The Late Cretaceous Bearpaw Formation in the South Saskatchewan River valley. Saskatchewan Research Council, Geology Division, Report No. 8. Caldwell, W.G.E., 1975. The Cretaceous System in the Western Interior of North America. Geological Association of Canada, Special Paper 13. Caldwell, W.G.E. and McNeil, D.H. 1981. Cretaceous Rocks and Their Foraminifera in the Manitoba Escarpment. Geological Association of Canada, Special Paper 21. Christiansen, E.A. 1967a. Geology and groundwater resources of the Saskatoon area (73- B). Saskatchewan Research Council, Geology Division, Map No. 7. Christiansen, E.A., 1967b. Collapse structures near Saskatoon, Saskatchewan, Canada. Canadian Journal of Earth Sciences, v.4: pp.757-767.

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Christiansen, E.A., 1968a. Pleistocene stratigraphy of the Saskatoon area, Saskatchewan, Canada. Canadian Journal of Earth Sciences, v.5: pp.1167-1173. Christiansen, E.A. 1968b. A thin till in west-central Saskatchewan Canada: Canadian Journal of Earth Sciences, v.5: pp. 329-336. Christiansen, E.A., 1977. Engineering properties of glacial deposits in southern Saskatchewan. Thirteenth Canadian Geotechnical Conference, Saskatoon, p. 30. Christiansen, E.A., 1979. The Wisconsinan deglaciation of southern Saskatchewan and adjacent areas. Canadian Journal of Earth Sciences, v.16: pp. 913-938. Christiansen, E.A., 1983. Geology of the Radisson Salinity Project, Saskatchewan. Saskatchewan Institute of Pedology. December 1983. Christiansen, E.A., 1990. Geology, in Christensen, E.A., ed. Physical environment of Saskatoon, Canada. Saskatchewan Research Council in Cooperation the National Research Council of Canada, NRC Publication 11378, pp. 3-17. Christiansen, E.A., 1992. Pleistocene stratigraphy of the Saskatoon area, Saskatchewan, Canada: an update. Canadian Journal of Earth Sciences, v.29, p. 1767-1778. Christiansen, E.A. and Sauer, E.K., 1994. Geotechnique of Saskatoon and surrounding area, Saskatchewan, Canada. Geological Association of Canada, Special Paper 42, pp. 117- 145. Christiansen, E.A. and Sauer, E.K., 1996. Geological Site Characterization Guidelines: a framework for Geohydrological and geotechnical applications in Saskatchewan. Saskatchewan Environment and Resource Management. Christiansen, E.A. and Sauer, E.K., 2001. Stratigraphy and structure of a Late Wisconsinan salt collapse in the Saskatoon Low, south of Saskatoon, Saskatchewan, Canada: an update. Canadian Journal of Earth Sciences, v.38, p.1601-1613. Domenico, P.A. and Schwartz, W., 1998. Physical and chemical hydrogeology. John Wiley and Sons, Inc., New York. Fraser, F.J., McLearn, F.D., Russell, L.S., Warren, P.S., and Wickenden, R.T.D., 1935. Geology of southern Saskatchewan. Geological Survey of Canada, Memoir 176, pp. 1– 137. Freeze, A.R. and Cherry, J.A., 1979. Groundwater. Prentice Hall Inc. ISBN 0-13-365312-9 Fortin, G, van der Kamp, G, and Cherry, J.A., 1989. Hydrogeology and Hydrocehmistry of an Aquifer-Aquitard System within Glacial Deposits, Saskatchewan, Canada. SRC Publication No. R-844-4-A-89. Gendzwill, D. and Stauffer, M., 2006. Shallow faults, Upper Cretaceous clinoforms, and the Colonsay Collapse, Saskatchewan. Canadian Journal of Earth Sciences, v.43, p.1859 1875.

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Gillies,J.A., and Middleton, B.B., 1986. Report on the Municipal Wells for the Village of Marcelin, Saskatchewan (SE06-46-06-W3). Golder Associates, 1985. Pumping Test Analysis Irrigation Water Supply Well Dalmeny, Saskatchewan. 852-6012. July 1985. Ho, A. and Barbour, S.L., 1987. Impact of potash tailings piles on groundwater. Report Prepared for Potash Corporation of Saskatchewan. International Water Supply Ltd., 1973. Biggar Replacement Well #1A. December 1973. International Water Supply Ltd., 1978. Village of Perdue Test Drilling – spring 1978 Water Sampling Program. December 1973. Jaques, D, 1989. Village of Speers Community Water Supply Phase 3 Report. Prepared by the PFRA, July 1989. J.D.Mollard and Associates Ltd., 1967. Village of Dalmeny Ground-water Investigation. December 1967. J.D.Mollard and Associates Ltd., 1968. Village of Dalmeny Report on Pump Well Installation. September 1968. J.D.Mollard and Associates Ltd., 1973. Report on Groundwater Exploration Program at Biggar, Saskatchewan Conducted for Canadian Department of Regional Economic Expansion Prairie Farm Rehabilitation Administration. July 1973. J.D.Mollard and Associates Ltd., 1976. Report on Installation of Well No.3A at Town of Biggar for Canadian Department of Regional Economic Expansion Prairie Farm Rehabilitation Administration. 1976. Keller, C.K., van der Kamp, G., and Cherry, J.A., 1988. Hydrogeology of two Saskatchewan tills, I. fractures, bulk permeability, and spatial variability of downward flow. Journal of Hydrology, 101, p. 97-121. Keller, C.K., van der Kamp, G., and Cherry, J.A., 1989. A multi-scale study of permeability of thick clayey till. Water Resources Research, 24 (11), 2299-2317. Kewen, T.J. and Schnieder, A.T., 1979. Hydrogeologic Evaluation of the Judith River Formation in West Central Saskatchewan. Saskatchewan Research Council G 79-2. March 1979. Krahn,J., Johnson, R.F., Fredlund, D.G., and Clifton, A.W., 1979. A highway cut Failure in Cretaceous sediments at Maymont, Saskatchewan. Canadian Geotechnical Journal. v16, pp. 703-715. Kruseman, G.P.; de Ridder, N.A. (1990). Analysis and Evaluation of Pumping Test Data (Second ed.). Wageningen, The Netherlands: International Institute for Land Reclamation and Improvement. ISBN 9070754207.

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Lebedin, J., 1989. Village of Denholm – Testhole Drilling. Prepared for the Prairie Farm Rehabilitation Administration by the Geology and Air Surveys Division of Saskatchewan Environment. File No. 4593-1 (2). December 1989. Lebedin, J., 1991. Village of Laird – Well Installation. Prairie Farm Rehabilitation Administration, File No. 4593-1 (2). December 1989. Leckie, D.A. and Cheel, R.J., 1989. The Cypress Hills formation (upper Ecocene to Miocene): A semi-arid braid plain deposit resulting from intrusive uplift. Canadian Journal of Earth Sciences, 26: pp. 1918 – 1931. Leckie, D.A., Bednarski, J.M., and Young, H.R., 2004. Depositional and tectonic setting of the Miocene Wood Mountain Formation, southern Saskatchewan. Canadian Journal of Earth Sciences, Volume 41, pp. 1319-1328. Lexicon of Canadian Geology (http://cgkn1.cgkn.net) Maathuis, H. and Schreiner, B.T., 1982. Hatfield Valley Aquifer System in the Wynyard Region, Saskatchewan. SRC Publication No. G-744-4-C-82. Maathuis, H. and van der Kamp, G., 1994. Subsurface brine migration at potash waste disposal sites in Saskatchewan. SRC Publication No. R-1220-10-E-94. Maathuis, H., 2005. Review of Pumping and Recovery Data for the Tyner Valley Aquifer and Impact of Pumping on the Tessier Aquifer. SRC Publication No. 10417-2E05. February 2005. Maathuis, H. and Famulak, M., 2007. Lessons Learned from the Impact of Pumping from Pre-Glacial Buried Valley Aquifer: a Case History – the Tyner Valley Aquifer near Saskatoon, Saskatchewan. OttawaGeo2007. Maathuis, H., and Simpson, M. 2007a. Groundwater resources of the Swift Current (72J) area, Saskatchewan. Saskatchewan Research Council, Publication 12178-1E07.

Maathuis, H., and Simpson, M. 2007b. Groundwater resources of the Wood Mountain (72G) area, Saskatchewan. Saskatchewan Research Council, Publication 12177-1E07.

Maathuis, H., and Simpson, M. 2007c. Groundwater resources of the Prelate (72K) area, Saskatchewan. Saskatchewan Research Council, Publication 11975-1E07.

Maathuis, H., and Simpson, M. 2007d. Groundwater resources of the Cypress Lake (72F) area, Saskatchewan. Saskatchewan Research Council, Publication 11974-1E07.

McLean, J.R., 1971. Stratigraphy of the Upper Cretaceous Judith River Formation in the Canadian Great Plains. Saskatchewan Research Council, Geology Division, Report No. 11. McNeil, D., and Caldwell, W., 1981, Cretaceous rocks and Their Foraminifera in the Manitoba Escarpment. Geological Association of Canada, Special Paper 21.

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MDH Engineered Solutions Corp., 2010a. Procedures for Regional Hydrogeological Mapping. Prepared for the Saskatchewan Watershed Authority. M1890-1030109. December 2010. MDH Engineered Solutions Corp., 2010b. Hydrogeological Investigation for the Saskatchewan Metals Processing Plant. Prepared for Fortune Minerals Limited. M2112-2840010. November 2010. Meneley, W.A. 1970. Geotechnology. Groundwater resources. In Christiansen, E.A. (ed.), Physical environment of Saskatoon, Canada. Saskatchewan Research Council, National Research Council of Canada, NRC Publication 11378, pp. 39-50. Meneley, W.A., 1972. Groundwater – Saskatchewan. In: Water supply for the Saskatchewan-Nelson Basin, Saskatchewan-Nelson Basin Report, Ottawa, Appendix 7, Section F, pp. 673 - 723. Misfeldt, G.A. 1988. An interactive slope stability and groundwater flow analysis of the Hepburn landslide. M.Sc. Thesis, department of Civil Engineering, University of Saskatchewan, Saskatoon Peterson, R. 1954. Studies of the Bearpaw Shale at a dam site in Saskatchewan. Proceedings of the American Society of Civil Engineers, Soil Mechanics and Foundation. Division, Volume 80. Roper Environmental Engineering Inc., 1992. North Canada Water Corp. Pump Test SW 14- 41-11 W3. Prepared for Elk Point Drilling Corp. EPD-169. February 1992. Saskatchewan Watershed Authority. Saskatchewan Watershed Authority. 2010. November 23, 2010. (http://www.swa.ca/). Sauer, E.K., Gareau, L.F., and Christiansen, E.A., 1990. Softening of overconsolidated Cretaceous clays by glacial erosion. Quarterly Journal of Engineering Geology, 23. Sauer, E. Karl, Egeland, A.K., and Christiansen, E.A., 1993. Compression characteristics and index properties of tills and intertill clays in southern Saskatchewan, Canada. Canadian Geotechnical Journal, 30. Schreiner, B., 2010. Geology and Groundwater of Southern Saskatchewan, Hydrogeological Mapping Protocol. SRC Publication No. 12831-1E10. Skwarawoolf, T., 1981. Biostratigraphy and paleoecology of Pleistocene deposits (Riddell Member, Floral Formation, late Rancholabrean). Canadian Journal of Earth Sciences, v.18: pp. 311-322. Stauffer, M., Gendzwill, D., and Sauer,E.K., 1989. Ice-Thrust Features and the Maymont Landslide in the North Saskatchewan River Valley. Canadian Journal of Earth Sciences, v.27, p.229-242. Stratigraphic Correlation Chart, Saskatchewan Ministry of Energy and Resources, revised 16 Nov. 2004. (http://www.ir.gov.sk.ca).

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Van Stempvoort, D., Ewert, L., and Wassenaar, L., 1992. AVI: a method for groundwater protection mapping in the Prairie Provinces of Canada. PPWB Report No. 114. Van Stempvoort, D., Ewert, L., and Wassenaar, L., 1993. Aquifer vulnerability index; a GIS- compatible method for groundwater vulnerability mapping. Canadian Water Resources Journal, Volume 18, No. 1, pp. 25-37. Viessman, Warren Jr. and G.L. Lewis, 1996. Introduction to Hydrology. 4th Ed. Addison- Wesley Education Publishers, Inc., NY. Vonhof, J.A., 1969. Tertiary gravels and sands in the Canadian Great Plains. Ph.D.Thesis, Department of Geological Sciences, University of Saskatchewan. Vrba, J., and Zaporozec, A., 1994. Guidebook on mapping groundwater vulnerability. International Association of Hydrogeologists, Volume 16, 131 p., Heise Verlag, Hannover. Whitaker, S.H., 1965. Geology of the Wood Mountain area (72-G) Saskatchewan. Ph.D.Thesis, University of Illinois, Urbana, Illinois. Whitaker, S.H. 1967. Geology and groundwater resources of the Wood Mountain area (72- G), Saskatchewan. Saskatchewan Research Council, Map No. 5. Whitaker, S.H. and Christiansen, E.A. 1972. The Empress Group in Southern Saskatchewan. Canadian Journal of Earth Sciences, V9. Whitaker, S.H., Irvine, J.A., Broughton, P.L., Cameron, A.R., and Sweet, A.R. 1978. Coal resources of southern Saskatchewan: a model for evaluation methodology: Geological Survey of Canada Economic Geology Report 30, Department of Mineral Resources 209, Saskatchewan Research Council Report 20.

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