EarthCache: Recharge and Flow — Water’s Underground Journey
Logging Tasks / Questions
To claim this EarthCache, please visit the posted coordinates and answer the following questions.
1. Geologic Setting
Question: The Judith River Formation beneath this site is made of ancient sandstones and siltstones. Why would these materials of the Judith River Formation make a good aquifer?
2. Glacial Influence
Question: The ground here is covered by glacial till. How might this layer help or hinder water recharge?
3. Aquifer Function
Question: How does groundwater in an aquifer differ from surface water in a pond or stream? Why is groundwater important to people and ecosystems?
4. Modern Recharge Connection
Think about: How could land use (paved surfaces, buildings, trails) in this area affect groundwater recharge today? Why do you think it’s important to keep recharge areas like this one covered with natural vegetation and forest instead of pavement or buildings?
Question: Based on your visit, would you say recharge at this site is fast, slow, or moderate? Explain your reasoning in one or two sentences.
5. Photo for Logging
Take a picture of yourself with the wetlands in the background(face optional), your GPSr, or a personal item at the site to show your visit.
Include it in your log after sending your answers to the Cache Owner.
DO NOT POST ANSWERS IN YOUR LOG. Please don’t provide the answers when logging the cache online except for the photo, for the rest of the queries use the “Send answers” feature OR geocache mail the cache owner including the earth cache GC number, title and the answers. 
Please answer to the best of your ability. As long as you give it your best effort, we'll be happy to accept your responses so you can log your EarthCache! You will probably find the answers you are looking for in this description page!
Location: West Swale Wetlands at Chappell Marsh north at Richard St. Barbe Baker Afforestation Area, Saskatoon, Saskatchewan. West Swale Wetlands at Chappell Marsh south at Chappell Marsh at Chappell Marsh Conservation Area
Coordinates: 52°06'00.2"N, 106°45'56.2"W
Theme: Groundwater recharge, aquifer formation, and the Judith River Formation
Region: South Saskatchewan River Basin
Earth Science Lesson: Recharge and Flow
Welcome to the Richard St. Barbe Baker Afforestation Area, a unique location where you can observe the link between rainfall, soil, and underground water. Beneath your feet lies a story millions of years in the making — one of ancient seas, glacial movement, and modern water cycles.
The Hidden Water Below
When rain or melting snow soaks into the ground, some of it flows downward past the roots of plants. This process is called infiltration, and it helps recharge aquifers — layers of rock and sediment that hold water. That underground water is called groundwater, and it slowly moves through spaces between grains of sand and gravel.
The Judith River Formation and Aquifer
The Judith River Formation, part of the Cretaceous Period (about 75 million years ago), stretches beneath parts of southern Alberta, Saskatchewan, and into the U.S. It formed when rivers, swamps, and coastal plains deposited sand, silt, and mud that later hardened into sedimentary rock.
These rocks are porous — full of tiny spaces — allowing water to flow through and store groundwater and create what we call the Judith River Aquifer, an important water source for farms and small communities in western Saskatchewan. Groundwater recharge is very important for cities like Saskatoon today.
This keeps wells and aquifers supplied with clean water, supports wetlands and rivers, and helps balance the effects of drought and heavy rainfall.
Water moves constantly through the environment, but not all of it runs off into streams and rivers. Much of it seeps quietly underground — a process known as groundwater recharge. Here, at the Richard St. Barbe Baker Afforestation Area, you are standing above a landscape shaped by glacial deposits and ancient Cretaceous bedrock formations that form part of the Judith River Aquifer system.
When rain or snowmelt infiltrates the soil, it percolates through layers of sand, silt, and glacial till until it reaches a saturated zone where all pore spaces are filled with water — the aquifer. The rate at which this recharge occurs depends on the permeability and porosity of the material below your feet.
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Glacial till (a dense, unsorted mixture of clay, silt, and gravel) slows infiltration.
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Sandy or silty deposits, on the other hand, allow faster percolation of water into the aquifer.
Beneath this area lies the Judith River Formation, a layer deposited during the Late Cretaceous (Campanian) period about 83.5 to 70.6 million years ago. It consists mainly of interbedded sandstone, siltstone, and mudstone, with occasional layers of coal and bentonite. These sediments — originally laid down in ancient river deltas and floodplains — now act as a regional aquifer that extends across southern Alberta and Saskatchewan into the northern United States.
In some areas of west-central Saskatchewan, the Judith River Aquifer provides a critical source of municipal and domestic water, connecting past geologic processes to today’s living communities.
Glacial Legacy and Recharge
During the last Ice Age, glaciers covered this land, leaving behind glacial till — a mix of clay, sand, gravel, and rock. Where till is sandy or gravelly, rainwater easily seeps in to recharge the aquifer below. Where clay layers exist, water cannot pass through quickly, slowing infiltration and creating perched water tables.
Water doesn’t just flow on the surface — it also travels underground. When rain or melted snow soaks into the soil, it begins a hidden journey called groundwater recharge. This process refills underground water stores known as aquifers.
Here, in the Richard St. Barbe Baker Afforestation Area, we are standing above a mix of glacial deposits and Cretaceous-age sandstone and mudstone belonging to the Judith River Formation. About 83 to 70 million years ago, this area was part of a coastal plain where dinosaurs roamed. The sediments they walked on have become a layer of interbedded sandstone, siltstone, and mudstone — materials that hold and move groundwater today.
As rain seeps through the upper layers of soil — topsoil, glacial till, and sandy deposits — it slowly recharges deeper formations such as the Judith River Aquifer. This aquifer extends beneath southern Saskatchewan and Alberta into the northern United States. In some rural areas, wells drilled into this aquifer provide clean drinking water for homes and towns.
Groundwater recharge is an invisible but vital part of the hydrologic cycle. The water that seeps through the soil here may one day emerge from a municipal well miles away — filtered naturally through ancient formations that once supported dinosaurs.
Understanding recharge areas like this one helps scientists and communities protect their underground water supplies, ensuring sustainable use of the Judith River Aquifer for future generations.
Groundwater vs. Surface Water:
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Groundwater is water stored underground in aquifers, filling the spaces between soil, sand, and rock.
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Surface water is found on the land surface in ponds, lakes, rivers, wetlands or streams.
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Groundwater moves slowly through underground layers, while surface water moves faster and is exposed to evaporation, sunlight, and temperature changes.
Importance of Groundwater:
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Provides drinking water for people and livestock.
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Supports irrigation for crops and water for industry.
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Feeds springs, streams, and wetlands, helping ecosystems survive during dry periods.
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Helps maintain base flow in rivers, keeping aquatic habitats healthy year-round.
In short, groundwater is a hidden but vital water source for both humans and nature.
Signs of Recharge in the Forest
At this location, you can observe how soil texture, vegetation, and landform reveal infiltration and recharge patterns:
Grassy, sandy areas = faster infiltration.
Clayey or compacted trails = slower infiltration.
Patches of cattails or willows = shallow groundwater or slow-draining soils.
Fast infiltration means more recharge potential. Slower infiltration shows where water might stay near the surface or run off.
COMPARISON OF RECHARGE RATES IN A VARIETY OF GREENSCAPE ECOSYSTEMS and GREYSCAPE LOCATIONS
Wetlands with Willows and Cattails
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Recharge Rate: Slow
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Why:
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Wetlands often have saturated soils — water already fills most of the pore spaces.
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The soils beneath (usually clays and silts) are fine-textured and less permeable, so water infiltrates slowly.
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Much of the water stays near the surface, moving laterally or evaporating instead of percolating downward.
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Vegetation like cattails and willows thrive in these saturated conditions and help retain water.
Grassland Meadows
Invasive Grass Meadows (e.g., Smooth Brome)
Recharge Rate: Slow to Moderate
Why:
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Dense, shallow root mats of smooth brome create a tight soil network that slows water infiltration.
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Monocultural stands reduce soil porosity compared to diverse native grass meadows.
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Aggressive rhizomes can compact upper soil layers, limiting deep water movement.
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Faster decomposition and nutrient cycling can increase surface runoff rather than promoting recharge.
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Overall, less precipitation soaks into the soil to reach aquifers compared to native grasslands.
Aspen Forest
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Recharge Rate: Moderate
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Why:
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Forest soils are rich in organic matter and have high infiltration capacity—especially under aspen, which promotes loamy soil.
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However, dense root networks and leaf litter absorb and retain moisture, so less may reach the aquifer compared to open grasslands.
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Transpiration rates in aspen are high—trees draw up a lot of groundwater and release it into the air.
Man-Made Surfaces (Greyscape: Streets, Sidewalks, Buildings, Houses, Other Structures)
In Summary (Fastest to Slowest Recharge):
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Native Moist Mixed Grassland Meadows – best for aquifer recharge. (Ponder this: The temperate grasslands are the world's most endangered ecosystem)
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Aspen Forest – moderate recharge; good infiltration but high uptake.
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Invasive Grass Areas (e.g., Smooth Brome) – slow to moderate; dense roots and monoculture reduce porosity and increase runoff.
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Wetlands with Willows and Cattails – slow; saturated fine soils limit infiltration.
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Man-Made Surfaces (streets, sidewalks, buildings) – very slow to none; water mostly runs off.
Location Evidence Observe your surroundings. What features at this location suggest that water can soak into the ground here (e.g., soil texture, vegetation, slope, or lack of standing water)? The soil looks loamy and dark, suggesting a mix of sand and silt with some organic matter. It crumbles easily, showing good infiltration potential. At GZ (ground zero -earth cache location) there is an ashpalt road called Township Road 362A (Cedar Villa Road) with gravel shoulders, so a hard area for soil testing. Then the gravel shoulders on both sides extend to the permanent class four wetlands by the road. However, if you walk on the paths in either of the greenspaces north or south, you may be able to experience the surroundings close up. Observe how trees and grasses differ depending on soil moisture.
Soil Texture Test If conditions allow, gently touch the soil or surface materials. Soil can feel sandy, silty, or clayey. Different soil types affect infiltration and recharge.
Infiltration Observation: If possible, pour a small amount of water onto the soil and observe. Observe how long does it take to soak in. Come to a conclusion about the ground’s permeability? It would soak in quickly because sandy or loamy soil has large spaces between particles that let water pass through easily. This is an interesting experiment, but not set as a task as winter conditions would prove this to be a hardship.
Hints
Look for low, sandy, or grassy areas where puddles don’t last long — those often indicate high infiltration.
Trails with compacted soil or puddles show low infiltration.
In winter, vegetation patterns reveal water flow paths. Have you ever noticed that snow melts first around tree bases and gentle slopes, showing warmer, more permeable ground where water seeps in rather than running off. Winter Alternative: What plants or landforms suggest that water often collects or moves through this area during warmer months?
Vegetation Indicator
Observe the vegetation to determine which plants dominate this spot (grasses, shrubs, trees, wetland species)? What might that tell you about the soil’s moisture level and recharge? Aspen trees and tall grasses suggest moderately moist soil that can support deep roots — typical of recharge zones where water moves downward. Trees grow where infiltration is strong and soil stays moist longer; grasses thrive in areas where the soil dries quickly after rain. Grasses and deep-rooted plants often indicate good infiltration; sedges and moisture-loving species may show poor drainage. Winter Observation: In winter, what signs show where water might move or collect beneath the snow? Snow melts first around tree bases and gentle slopes, showing warmer, more permeable ground where water seeps in rather than running off. Seasonal Changes: Recharge rates differ between spring, summer, fall, and winter. Spring snowmelt causes the most recharge; summer heat dries soil faster; fall rains may recharge again; winter is slowest due to frozen ground.
In this way, the Richard St. Barbe Baker Afforestation Area wetlands acts like a living classroom — showing how nature filters and stores clean water underground.
SUMMARY Recharge and Flow: Water’s Underground Journey
When rain or snow melts, some of that water runs off into streams — but some soaks in.
That soaking-in is called infiltration, and it helps refill the underground layers of rock and sand known as aquifers.
Here in Saskatoon, the Judith River Aquifer lies deep below the ground. It was formed about 75 million years ago from rivers and swamps that once flowed across this region.
Glaciers later covered the land, leaving behind a blanket of glacial till — sand, clay, and gravel that control how quickly water can move into the earth.
By watching how the land holds or releases water, we can see the connection between today’s rainfall and tomorrow’s drinking water.
Earth Science Extension — Protecting Groundwater for the Future
The water that seeps into the soil at the Richard St. Barbe Baker Afforestation Area doesn’t stop there — it continues its slow underground journey. Over many years, it may reach deep sandstone layers belonging to the Judith River Aquifer, part of a system of ancient river and delta sediments that formed over 70 million years ago during the time of the dinosaurs!
This aquifer stretches across parts of Saskatchewan, Alberta, and Montana, storing fresh water in porous rock layers between less permeable clay and shale. Such aquifers are vital — they act as natural underground reservoirs that provide safe drinking water for communities and maintain base flow in rivers during dry seasons.
The City of Saskatoon and the Water Security Agency of Saskatchewan carefully monitor groundwater recharge areas like this one. Protecting these zones from contamination (for example, from stormwater runoff or development) helps ensure that clean water remains available for generations.
Vegetation helps water soak into the soil and filter out pollutants before it reaches the aquifer. If the land were paved or developed, rain would run off instead of recharging the groundwater, and contamination risks would increase.
The story of groundwater is the story of connection — between rainclouds and wells, roots and rivers, past and present. The same processes that once buried dinosaur bones now help store water for life today. By learning about recharge zones like this one, we can help protect our underground water for generations to come.
Oh! and here is news about the Civic Operations Centre located east of Richard St. Barbe Baker Afforestation Area along Township Road 362A
Proactive Measures for Protecting Groundwater Recharge at the Civic Operations Centre
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Controlled Snow Melt Management: Snow collected from streets and city surfaces is stored in a designated "Snow Storage Decontamination Facility," where meltwater is carefully managed to prevent uncontrolled runoff.
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Oil and Grit Separation: As snow melts, water flows through an oil and grit separator, removing pollutants such as hydrocarbons and suspended solids before entering the stormwater system.
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Baffle Curtains and Settling Ponds: Meltwater passes through multiple baffle curtains and a settling pond, where sand, gravel, and debris are captured, reducing sediment and contaminant load.
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Salt, Sand, and Debris Removal: The facility ensures that salt, sand, gravel, and other urban contaminants are removed before meltwater is released, protecting water quality.
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Monitored Release: The treated meltwater is carefully monitored and only released into the stormwater system when appropriate, ensuring controlled flow and minimizing potential impacts on the Judith River aquifer.
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Environmental Stewardship: By treating and controlling snow melt, the facility reduces pollutant transport, prevents aquifer contamination, and contributes to the City’s commitment to sustainable water management.
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Aquifer Recharge Protection: These measures help maintain the quality of water that percolates into the ground, supporting the natural recharge of the Judith River aquifer and safeguarding water resources for people and ecosystems.
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Write a letter Compliment the City for the proactive environmental measures taken at the Snow Storage Decontamination Facility and for the benefits of the Richard St. Barbe Baker Afforestation Area and George Genereux Urban Regional Park which both help recharge the Judith River Formation.
APPENDIX
According to Environmental Dynamics Incorporated EDI who did an assessment of the soils in RSBBAA, the results are on page 6 Section 2.1.3
Within the Study Area of RSBBAA, six soil associations and eight soil map units were mapped, with the Elstow and Tuxford associations dominating. These soils—primarily Dark Brown Chernozems with Solonetzic variants such as Solonetz and Solod on lower slopes—have moderately severe agricultural limitations because of low moisture-holding capacity and weak structure. Wind-erosion risk varies from low on the loam-rich soils in the north to high on the sandy Asquith soils in the southeast, particularly in SE 13-36-06 W3M and along the western edge of the West Swale. Water-erosion potential is minimal across the area thanks to gentle slopes and sandy-loam textures, and stoniness was not classified.
WSP assessment reports that the site chiefly underlain by Bradwell soils, with smaller areas of Asquith and Meadow soils, and each presents specific limitations. Bradwell and Asquith soils—derived from lacustrine loam and fluvial sandy loam, respectively—both have low water-holding capacity that restricts crop options and the productivity of perennial forage species. Meadow soils, formed from alluvial sandy loam, have the opposite challenge: excess moisture caused by poor drainage or a high water table, limiting them to native forage production. The area also includes Asquith–Bradwell complex soils, a very fine sandy clay loam developed from mixed fluvial and lacustrine parent materials. This is the Golder Associates report for this area
Asquith Soils Asquith soils are sandy, rapidly draining Dark Brown Chernozems that dry out quickly and are highly susceptible to wind erosion. Their coarse texture limits nutrient retention and moisture availability.
Elstow Soils Elstow soils are Dark Brown Chernozems with moderate limitations for agriculture, characterized by low moisture-holding capacity and relatively weak structure, typically forming on loamy to clay loam glacial till.
Meadow soils Meadow soils are poorly drained, moisture-rich soils—often Gleysolic—that form in low-lying areas where groundwater is high or water accumulates, resulting in saturated conditions that limit crop options and favour native wetland or moisture-tolerant vegetation.
Tuxford Soils Tuxford soils are also Dark Brown Chernozems but often include Solonetzic features—such as hard, dense B horizons—that restrict root growth and water movement. These soils have moderate to severe limitations due to poor structure and reduced available water.
Glossary of Geological Terms
Term Definition
Alluvial Materials Alluvial materials are similar to fluvial deposits but refer more broadly to sediments laid down by running water in floodplains, fans, or deltas. They are typically well-sorted, fertile, and variable in texture.
Aquifer A layer of rock or soil underground that can hold and carry water. Aquifers act like a sponge, storing water that people can pump out for drinking or farming.
Chernozems Chernozems are fertile grassland soils characterized by a dark, organic-rich surface horizon, good structure, and high natural nutrient levels, formed under prairie vegetation in semi-arid to subhumid climates.
Erosion: When soil, rocks, or sand are worn away by wind, rain, or moving water.
Fluvial Materials
Fluvial materials are sediments deposited by flowing water in rivers or streams. These deposits are often sorted by grain size and can include sands, silts, and gravels.
Glacial Till A mix of clay, sand, and rock left behind when glaciers melted. Till covers much of the Saskatoon area and affects how water moves through the ground.
Groundwater Water that fills the cracks and spaces between soil and rocks below the Earth’s surface. It moves slowly through the ground and is part of the water cycle.
Infiltration The process of water soaking down into the ground. When water from rain or snow seeps down through the soil into the ground instead of running off the surface.
Intermittent Stream:
A stream that only has water during certain times of the year, such as after heavy rains or snowmelt.
Judith River Formation A layer of ancient sedimentary rock sandstones and siltstones formed during the time of the dinosaurs (about 75 million years ago). It holds water in western Saskatchewan and is part of the Judith River Aquifer.
Lacustrine Materials Lacustrine materials are fine-textured sediments, such as silts and clays, deposited at the bottom of ancient or existing lakes. These materials tend to have good water-holding capacity but may be dense when dried.
Perennial Stream: A stream that has flowing water all year long.
Permeability How easily water moves through a rock or soil. Sand has high permeability (water flows through easily), while clay has low permeability (water moves very slowly).
Porosity How much empty space a rock or soil has for holding water. The more space there is, the more water it can hold.
Recharge When rain or melted snow soaks into the ground to refill the aquifer. The process when rain or melting snow soaks into the ground and adds water to the aquifer.
Riparian Zone:
The green area of plants and trees along the edge of a stream, river, or wetland. It helps prevent erosion and filters water before it enters the stream
Sedimentary Rock Rock made from layers of mud, sand, and fossils pressed together. Many aquifers form in these rocks.
Soil Horizon:
The different layers you can see in a soil profile — topsoil, subsoil, and deeper parent material. Each layer has different colors and textures.
Solonetzic Soils
Solonetzic soils are characterized by high sodium levels in the subsoil, resulting in a dense, hard B horizon that restricts root growth, limits water movement, and creates significant structural challenges for plant productivity.
Watershed The area of land where all water drains into one place such as a river, lake, or aquifer..
The following images are schematic diagrams of aquifers.
The Judith River Formation acts as a regional aquifer in parts of southwestern and west-central Saskatchewan and neighboring regions. Its characteristics can vary locally, but generally:
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Type: It is typically considered a confined aquifer where it is overlain by less permeable layers (e.g., shales or clay-rich sediments), meaning the water is under pressure.
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Unconfined zones: In areas where overlying sediments are more permeable or thin, parts of the aquifer may behave as unconfined, allowing water to directly infiltrate from the surface.
So, the Judith River Formation is mostly confined, but local variations can create unconfined conditions in some locations.
Fracking can potentially affect the Judith River Formation aquifer, though the risk depends on the depth of drilling, the geology, and the integrity of well casings. Here’s a clear breakdown:
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Depth factor: The Judith River Formation aquifer is a regional groundwater source, often shallower than many fracking zones, which usually target deeper shale layers. If fracking occurs above or near the aquifer, there is a risk of contamination.
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Well integrity: Properly constructed and sealed wells minimize the chance of fracking fluids leaking into the aquifer. Poorly cased wells can create pathways for chemicals or methane to reach groundwater.
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Hydraulic fracturing fluids: These fluids contain chemicals that, if they migrate upward, could alter water quality in the aquifer.
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Induced fractures: In most cases, the fractures are designed to stay deep underground, far below the aquifer, but if geology allows upward migration along faults or fractures, contamination is possible.
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Monitoring: Regulatory frameworks and testing of aquifer water quality are used to detect and prevent contamination.
In summary: With careful drilling and regulation, the Judith River aquifer is usually protected, but improper fracking or unexpected geological pathways could impact it.
Diagram of an aquifer illustrating areas of confined groundwater, the movement of water over time, and locations of a spring and a well.
Above Confined continental coastal aquifer without seepage zone Gabriel HY Lam cc 4.0
Above An aquifer cross-section. This diagram shows two aquifers with one aquitard (a confining or impermeable layer) between them, surrounded by the bedrock aquiclude, which is in contact with a gaining stream Hans Hillewaert cc 3.0
Bibliography
Agriculture and Agri-Food Canada. The Soils of the Saskatoon Map Area (73-B). Canadian Soil Information Service, n.d. https://sis.agr.gc.ca/cansis/publications/surveys/sk/sks4/sks4_report.pdf
. Accessed 26 Oct. 2025.
City of Saskatoon. South Saskatchewan River Watershed and Groundwater Overview. City of Saskatoon, n.d. https://www.saskatoon.ca
. Accessed 26 Oct. 2025.
Geological Society of America. EarthCache Guidelines. GSA, n.d. https://www.geosociety.org/GSA/GSA/fieldexp/EarthCache/guidelines/home.aspx
. Accessed 26 Oct. 2025.
Government of Canada. Sediment Yield and Bank Stability in Prairie River Systems. Environment Canada, 1988. https://publications.gc.ca/collections/collection_2021/eccc/en37/En37-352-1988-eng.pdf
. Accessed 26 Oct. 2025.
Kewen, S., and Schneider, R. Judith River Aquifer Hydrogeology in West-Central Saskatchewan. Geological Survey of Canada, 1979. https://geoscan.nrcan.gc.ca
. Accessed 26 Oct. 2025.
Li, L. Sediment Transport Modelling of the South Saskatchewan River. University of Saskatchewan, 2024. HARVEST Digital Repository, https://harvest.usask.ca/bitstreams/730ce8f1-0400-4c1a-b0b0-40bfbc967622/download
. Accessed 26 Oct. 2025.
Parks Canada Research Centre. South Saskatchewan River Basin Biogeography. IACC, 2004. https://www.parc.ca/mcri/pdfs/SSRBbiogeography.pdf
. Accessed 26 Oct. 2025.
Whitaker, S. Hydrogeology of the Judith River Formation in Southwestern Saskatchewan. Government of Saskatchewan, 1982. https://publications.saskatchewan.ca
. Accessed 26 Oct. 2025.
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