10.2 Drainage Basins

Cawston Creek near Keremeos, B.C. The line circling Cawston Creek shows the extent of the drainage basin. A dashed line shows the drainage basin of one of its tributaries
Figure 10.4 Cawston Creek near Keremeos, B.C. The blue line shows the extent of the drainage basin. The dashed red line is the drainage basin of one of its tributaries. Image descriptions at end of chapter. Cawston Creek is a drainage basin made up of a number of small streams that flow into the Similkameen River. The Cawston Creek drainage basin also has a smaller tributary drainage basin that flows into it.

A stream is a body of flowing surface water of any size, ranging from a tiny trickle to a mighty river. The area from which the water flows to form a stream is known as its drainage basin. All of the precipitation (rain or snow) that falls within a drainage basin eventually flows into its stream, unless some of that water is able to cross into an adjacent drainage basin via groundwater flow. An example of a drainage basin is shown in Figure 10.4

Figure 10.5 Profile of the main stem of Cawston Creek near Keremeos, B.C. The maximum elevation of the drainage basin is about 1,840 meters, near Mount Kobau. The base level is 275 meters, at the Similkameen River. As shown, the gradient of the stream can be determined by dividing the change in elevation between any two points (rise) by the distance between those two points (run). Image descriptions at end of chapter.

Cawston Creek is a typical small drainage basin (approximately 25 square kilometers) within a very steep glaciated valley. As shown in Figure 10.5, the upper and middle parts of the creek have steep gradients (averaging about 200 meters per kilometer but ranging from 100 to 350 meters per kilometer), and the lower part, within the valley of the Similkameen River, is relatively flat (less than 5 meters per kilometer). The shape of the valley has been controlled first by tectonic uplift (related to plate convergence), then by pre-glacial stream erosion and mass wasting, then by several episodes of glacial erosion, and finally by post-glacial stream erosion. The lowest elevation of Cawston Creek (275 meters at the Similkameen River) is its base level. Cawston Creek cannot erode below that level unless the Similkameen River erodes deeper into its flood plain (the area that is inundated during a flood).

Metro Vancouver’s water supply comes from three large drainage basins on the north shore of Burrard Inlet, as shown in Figure 10.6. This map illustrates the concept of a drainage basin divide. The boundary between two drainage basins is the height of land between them. A drop of water falling on the boundary between the could flow into either one of them.

Figure 10.6 Drainage Basins of Vancouver, Canada, Credit: Google Earth

The pattern of tributaries within a drainage basin depends largely on the type of rock beneath, and on structures within that rock (folds, fractures, faults, etc.). The three main types of drainage patterns are illustrated in Figure 10.7 Dendritic patterns, which are by far the most common, develop in areas where the rock (or unconsolidated material) beneath the stream has no particular fabric or structure and can be eroded equally easily in all directions. Examples would be granite, gneiss, volcanic rock, and sedimentary rock that has not been folded. Most areas of British Columbia have dendritic patterns, as do most areas of the prairies and the Canadian Shield. Trellis drainage patterns typically develop where sedimentary rocks have been folded or tilted and then eroded to varying degrees depending on their strength. The Rocky Mountains of B.C. and Alberta are a good example of this, and many of the drainage systems within the Rockies have trellis patterns. Rectangular patterns develop in areas that have very little topography and a system of bedding planes, fractures, or faults that form a rectangular network. Rectangular drainage patterns are rare in Canada.

Figure 10.7 Typical dendritic, trellis, and rectangular stream drainage patterns. Drainage patterns: Left, Dendritic: a pattern of drainage channels that resembles the branches in a tree. Middle, Trellis: a drainage pattern in which tributaries typically flow parallel to one other but meet at right angles. Right, Rectangular: a drainage pattern in which tributaries typically flow at right angles to each other and meet at right angles.

In many parts of Canada, especially relatively flat areas with thick glacial sediments, and throughout much of Canadian Shield in eastern and central Canada, drainage patterns are chaotic, or what is known as deranged (Figure 10.8, left). Lakes and wetlands are common in this type of environment.

Figure 10.8 Left: a typical deranged pattern; right: a typical radial drainage pattern developed around a mountain or hill.  Left image, Deranged, with no coherent pattern, common in post-glacial environments. Right image,  Radial, streams draining water from a mountain, often a volcano.

A fourth type of drainage pattern, which is not specific to a drainage basin, is known as radial (Figure 10.8, right). Radial patterns form around isolated mountains (such as volcanoes) or hills, and the individual streams typically have dendritic drainage patterns.

Over geological time, a stream will erode its drainage basin into a smooth profile similar to that shown in Figure 10.9. If we compare this with an ungraded stream like Cawston Creek (Figure 10.5), we can see that graded streams are steepest in their headwaters and their gradient gradually decreases toward their mouths. Ungraded streams have steep sections at various points, and typically have rapids and waterfalls at numerous locations along their lengths.

Figure 10.9 The topographic profile of a typical graded stream. While the topographical profile of Cawston Creek fell at a steady rate and then leveled out for the last three kilometers, the topographical profile of a typical graded stream starts out steep, but the slope (or gradient) gradually decreases towards the bottom to form a soft curve.

A graded stream can become ungraded if there is renewed tectonic uplift, or if there is a change in the base level, either because of tectonic uplift or some other reason. As stated earlier, the base level of Cawston Creek is defined by the level of the Similkameen River, but this can change, and has done so in the past. Figure 10.10 shows the valley of the Similkameen River in the Keremeos area. The river channel is just beyond the row of trees. The green field in the distance is underlain by material eroded from the hills behind and deposited by a small creek (not Cawston Creek) adjacent to the Similkameen River when its level was higher than it is now. Sometime in the past several centuries, the Similkameen River eroded down through these deposits (forming the steep bank on the other side of the river), and the base level of the small creek was lowered by about 10 meters. Over the next few centuries, this creek will seek to become graded again by eroding down through its own alluvial fan.

Figure 10.10 An example of a change in the base level of a small stream that flows into the Similkameen river near Keremeos. The previous base level was near the top of the sandy bank. The current base level is the river (hidden behind the trees) which has eroded down into the sandy deposit.

Another example of a change in base level can be seen along the Juan de Fuca Trail on southwestern Vancouver Island. As shown in Figure 10.11, many of the small streams along this part of the coast flow into the ocean as waterfalls. It is evident that the land in this area has risen by about 5 meters in the past few thousand years, probably in response to deglaciation. The streams that used to flow directly into the ocean now have a lot of down-cutting to do to become regraded.

Figure 10.11 Two streams with a lowered base level on the Juan de Fuca Trail, southwestern Vancouver Island.

The ocean is the ultimate base level, but lakes and other rivers act as base levels for many smaller streams. We can create an artificial base level on a stream by constructing a dam, as illustrated in Exercise 10.2.

Exercise 10.2 The effect of a dam on base level

Figure 10.12 Revelstoke Dam and Revelstoke Lake on the Columbia River at Revelstoke, BC.

When a dam is built on a stream, a reservoir (artificial lake) forms behind the dam.  This temporarily (for many decades at least) creates a new base level for the part of the stream above the reservoir.

How does the formation of a reservoir affect the stream where it enters the reservoir, and what happens to the sediment it was carrying?

The water leaving the dam has no sediment in it. How does this affect the stream below the dam?

Sediments accumulate within the flood plain of a stream, and then, if the base level falls, or if there is less sediment to deposit, the stream may cut down through those existing sediments to form terraces. A terrace on the Similkameen River is shown in Figure 10.10 and some on the Green River are shown in Figure 10.13

Figure 10.13 This view is looking downstream (south) along the Green River from the Split Mountain Overlook in Dinosaur National Monument. The modern river channel expands to cover the entire flood plain in times of high flow, particularly during the spring snow melt. The construction of the high dam in Flaming Gorge has significantly altered the natural discharge of the Green River, but the Yampa River and other regional streams still retain most of their uncontrolled natural flow. This view shows two stream terraces on the left bank of the river, and two higher terraces are visible on the flanks of Blue Mountain in the distance. The 1st Terrace is about 40 feet above river level, the 2nd Terrace is about 120 feet above stream level. A 3rd Terrace forms a flat bench above some low cliffs along the river in the distance and is about 350 feet above stream level, and a 4th Terrace is about 700 feet above stream level. The degree of erosional degradation of each of the terraces increases with each higher (and older) terrace (USGS is licensed by Public Domain). Image Source

In the late 19th century, American geologist William Davis proposed that streams and the surrounding terrain develop in a cycle of erosion (Figure 10.14). Following tectonic uplift, streams erode quickly, developing deep V-shaped valleys that tend to follow relatively straight paths. Gradients are high, and profiles are ungraded. Rapids and waterfalls are common. During the mature stage, streams erode wider valleys and start to deposit thick sediment layers. Gradients are slowly reduced and grading increases. In old age, streams are surrounded by rolling hills, and they occupy wide sediment-filled valleys. Meandering patterns are common.

Davis’s work was done long before the idea of plate tectonics, and he was not familiar with the impacts of glacial erosion on streams and their environments. While some parts of his theory are out of date, it is still a useful way to understand streams and their evolution.

Figure 10.14 A depiction of William Davis’s cycle of erosion shown clockwise from stages a through d. Initial stage (a): A tectonic uplift forms two sharp valleys on each side. Youthful stage (b) : Steams flowing through those valleys erode the surrounding earth quickly and cut deep to form sharp V’s. Mature stage (c): The streams become wider and the banks more gradual. This marks the initial development of a flood plain. Old age (d): Steams for a wide flood plain where little erosion occurs.

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10.2 Drainage Basins Copyright © 2021 by Katharine Solada and K. Sean Daniels is licensed under a Creative Commons Attribution 4.0 International License, except where otherwise noted.

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