Channel Morphology and Classification

2 years ago

Atiqur Rahman

17 minutes

Channel Morphology

The study of channel-related aspects like channel pattern, channel geometry and the factors controlling these forms is called Channel Morphology. The factors that govern and affect the channel are the processes by which a channel is modified. The channel morphology also includes studying the network of tributaries that join the main river channel within the drainage basin.

Channel development is controlled by two factors:

Water flow or discharge (in terms of Volume and velocity) and
Sediment movement

These two factors are governed by the channel slope or gradient. The channel gradient varies from steep to gentle slope depending on the altitudinal variation that a channel is crossing by.

The mutual inter-relation of these parameters may be qualitatively described by Lane’s Principle (also known as Lane’s relationship) that states the product of the sediment load and bed grain size is proportional to the product of discharge and channel slope.

Definition of Channel

The term channel is used to define the path of a narrow water body such as a river or a strait. Thus, in Physical Geography, Channel can be defined as the path of a river or a stream outlined by its bed and banks.

The whole system of river channels with their joining branches in the form of tributaries that dissect the earth’s surface is in proportion to the valley size. Channels are occupied by permanent streams that flow throughout the year, some have intermittent streams, and some have ephemeral streams, which are active only during and after the rains.

Although the water of the river flows in its channel during floods, the water flow exceeds the capacity of the channel, and the water spills out of the channel over the floodplain, causing a flood.

The term channel is often synonymous with the term strait, which is defined as a relatively narrow body of water that connects two larger bodies of water. In this nautical context, the term strait, channel and passage are used interchangeably.

For example, in an archipelago, the water between islands is typically called a channel or passage. Similarly, for example, The English Channel is the strait between England and France.

Channel Structure

Channel Structure consists of Channel banks, Channel bed and Thalweg.

Channel Bed: The main path the river takes through which it flows is called the channel bed.

Channel Banks: The two sides of the river bed are called channel banks.

Thalweg: It is a continuous line joining the lowest points in a stream channel.

Factors Controlling Channel Morphology

There are two sets of factors that control channel morphological aspects such as channel pattern and channel movement.

Independent Factors

These are the factors that are imposed on the watershed. These are related to landscape aspects and control channel morphology such as geology, climate, and human (Figure).

The geology of a watershed is determined by processes acting on the landscape and can include endogenic processes such as volcanism, tectonics, and, to a lesser extent, surface processes such as erosion and deposition. Within a watershed, these processes control the distribution, structure and type of bedrock, surficial materials, and topography (Montgomery 1999).

The climate is also considered as an independent factor at the landscape scale as it is decisive in controlling the amount of rainfall and water flow in the stream channels. Human actions on the landscape can also significantly alter the watershed conditions.

The geologic, climatic, and human conditions to which a watershed is subjected determine the dependent landscape variables of sediment supply, stream discharge, and vegetation (Montgomery and Buffington 1993; Buffington et al. 2003).

An additional important independent variable is time.

Dependent Factors

These are those variables that respond and adjust to the independent conditions. Channel morphology results from the combined influence of these dependent landscape variables and the channel responses to changes in these variables by adjustments in one or many of the dependent channel variables (Figure).

The frequency, volume, and calibre of material delivered to the channel determine the sediment supply. Stream discharge includes the frequency, magnitude, and duration of stream flows. The variability in stream discharge, both temporally and spatially, exerts a large influence on channel morphology.

The third variable that influences the channel is riparian vegetation which controls bank erodibility as well as near-bank hydraulic conditions and is also a source of in-channel large woody debris (LWD).

Classic models depicted channel morphology as primarily a function of streamflow and sediment transport rate, where transport rate equals sediment supply for equilibrium conditions (e.g., Schumm 1971).

But these models did not explain the role of vegetation or other boundary conditions, which are crucial in determining channel morphology. Besides riparian vegetation, important boundary conditions include elements found within the stream channel, as well as those that may influence the channel’s ability to migrate laterally and (or) build vertically.

The most important boundary conditions include the following:

Channel gradient that is controlled by valley slope, as the maximum possible gradient that a stream channel can have, is dependent on valley slope; and

Bank composition and structure, which influence bank erodibility as determined by the sedimentology and geotechnical properties of the material bounding the channel;

Bedrock and other non-erodible units (such as colluvial material, compact tills, and lag glaciofluvial deposits), which may limit lateral and vertical channel migration and determine stream channel alignment;

Erodible sediment stored in valley bottoms in floodplains, fans, or terraces (including alluvial sediments; lacustrine, marine, and glacial outwash deposits; and fine-textured colluvium);

Human channel alterations, such as bridge crossings and flood protection works.

These boundary conditions are primarily influenced by the geomorphic history of a landscape, as well as the history of human intervention. Therefore, the current morphology of a stream is a product of present-day and historic watershed processes.

Channel Classification

The channels can be classified into different categories based on different criteria. These criteria include the constituent material of the river channel and the shape or pattern of the river channel. The pattern of the channel is described as channel form. Channels exist in a variety of forms.

There are a wide variety of stream channel types based on their forms, such as Single Thread Sinuous rivers, Wandering rivers or a meandering river, Braided rivers, etc., enclosed by the materials of their bed and banks.

Bedrock Channel

When the river bed has a cover of rocks rather than sediment cover and the river erodes into the rock. These are the channels that flow through non-erodible materials (e.g., bedrock, coarse colluvium, and non-erodible glacial deposits), and their boundary conditions tend to dominate the channel morphology.

This type of channel usually has a limited sediment supply and a morphology that is largely determined by the structure and composition of the material through which it flows. Bedrock channels, for example, frequently run along faults or other geologic planes of weakness within the rock.

Overall, these channels are relatively insensitive to disturbances, including disturbances from changes occurring upstream (i.e., the channel is relatively stable), but bedrock channels are very effective at transferring disturbances from upstream to downstream reaches.

Alluvial Channel

When the river cuts the river-transported rock debris or alluvium, this is referred to as the alluvium channel. These channels are more regular.

Schumm (1985) has proposed a more detailed channel classification that included three categories: (1) bedrock channel, (2) semi-controlled channel, and (3) alluvial channel, but this classification was found not to address the variable geotechnical properties associated with the landforms.

So Kellerhals et al. 1976, has suggested that the categories should be based on the materials that determine channel bed and bank strength and the channel’s threshold of erodibility. Based on this, three categories of materials constituting channels could be identified (1) non-erodible, (2) semi-erodible, and (3) erodible.

Although these terms (as opposed to the conventional “nonalluvial” and “alluvial”) are more useful, by definition, these are contradictory, as all alluvial material is erodible and many non-alluvial materials are also highly erodible (e.g., marine and glaciofluvial deposits).

Similarly, some alluvial materials are far less erodible than others; for instance, armoured channel beds developed by fluvial processes are much more resistant to movement than other alluvium, such as gravel-bar deposits, which are rearranged on an annual basis.

The other classification is based on the shape assumed by the river channel, called a planform pattern. In the words of Leopold (1957), “Channel pattern is used to describe the plan view of a reach of river as seen from an aeroplane and includes meandering, braiding or relatively straight channels.

Natural channels characteristically exhibit alternating pools or deep reaches and riffles or shallow reaches, regardless of the type of pattern.” The shape of the channel is largely decided by the sinuosity of the river.

Sinuosity refers to the ratio of the measured channel distance divided by the valley’s straight-line distance from the channel reach’s beginning to the end of the channel reach.

Mollard (1973) identified 17 planform channel types that were related to both the physiographic environment in which channels flowed and the materials that made up the channel bed and banks. He based this channel pattern classification on the factors controlling morphology, specifically streamflow, sediment supply, the relative dominance of fluvial transport processes, and the materials within which the channel is formed.

Church (1992) classified channel patterns based on the calibre and volume of sediment supply that, in turn, decides the sinuosity of the river channel. He has separated the patterns into phases of river channel flow during its upper course to lower course, related to how the supplied sediment gets transported.

On a more simplistic scale, channels can be categorized into four types based on the pattern taken by the river channel.

Channel Types on the basis of Pattern — Channel Types on the Basis of Pattern

Straight River Channel

For channels with moderate-sized bed material (such as gravel-bed streams), channels with moderate sediment supply usually have a “straight river channel”.

Sinuous River Channel

As the channel bends slightly with the increase in the sediment load, the channel is called a “sinuous river channel”.

Meandering River Channel

As the supply of sediments exceeds the channel’s capacity to transport the additional sediment, the channel may take a zig-zag shape called a “meandering channel”. The channel may break into two or more individual channels. When the channel is not too active, it can divide and recombine around stable, vegetated islands; these are called wandering channels.

Braided River Channel

In other situations, the channel becomes too active for stable vegetated islands to develop, and the system divides into numerous individual channels that divide and recombine around unstable gravel bars; these are called “braided channels.”

Anastomosing rivers or streams are similar to braided rivers in that they consist of multiple interweaving channels but they typically consist of a network of low-gradient, narrow, deep channels with a stable bank.

Hydraulic Geometry of Stream Channels

The analysis of the relationship among stream discharge, channel shape, sediment load and slope is called the hydraulic geometry of stream channels.

Gaging stations around the world maintained by the respective governments make recordings along the rivers all over the world. At these stations, the water surface level, channel shape, stream velocity, amount of dissolved and suspended minerals and other variables are periodically recorded.

These records provide a detailed history of river flow. In 1953, L.B. Leopold and Thomas Maddock published an elaborate analysis of thousands of measurements from stream gaging stations all over the world. It was they who called their analysis of the relationship among stream discharge, channel shape, sediment load and slope as hydraulic geometry of stream channels.

To understand the hydraulic geometry of stream channels, there is a need to study the changes in the following four parameters-

channel width and depth,
stream velocity, and
suspended load

At different gaging stations under varying conditions spanning from low flow to bank full discharge and flood. These four parameters increase as some small, positive power function of discharge based on the following equations:

w = aQ^b d = cQ^f v = kQ^m

where

Q stands for water discharge

w refers to the water surface width

d stands for mean water depth, and

v is the mean current velocity

The numerical values for arithmetic constants a,c, and k are not very significant for the hydraulic geometry of stream channels. They are constants of proportionality that convert a given value of discharge into the equivalent values of width, depth and velocity. The numerical values of the exponents b, f and m are very important as they describe the changes in width, depth and velocity for a specified change of discharge are very important.

During the flood, the water rises and stream channel width, depth and current velocity all increase at the gaging stations. This is clearly evident during the flood situation, as the regularity of the average changes drastically.

In a downstream direction, the changes in channel shape and stream velocity are more significant, as was emphasised by Leopold and Maddock in 1953. River discharge in humid areas increases downstream. They proved that as the mean discharge of a river increases downstream, channel width, channel depth, and mean current velocity all increase.

Leopold and Maddock showed that not only do the effluent rivers get both wider and deeper as they grow larger downstream, but against popular belief, they also proved that average current velocity increases downstream. This is because the high-velocity current in the upper course of the river flows in circular eddies, with backwards as well as forward motion. Are not the same.

B = 0.5, f = 0.4, and m = 0.1

These values show that channel width increases most rapidly with mean annual discharge (as the square root of the discharge), depth next most rapidly, and mean velocity increases only slightly in the downstream direction.

Leopold and Maddock proposed that the increasing depth downstream permits more efficient flow in a river and compensates for the decreasing slope, thus providing a slight net increase in velocity at mean annual discharge.

Thus, the channel width, depth and velocity change with the stream flow. And against popular belief, the velocity increases though only slightly in the downstream direction.

Channel Stability and Movement

“Channel Stability” refers to the channel’s propensity for vertical or lateral movement (Church 2006). Channel stability keeps on changing as the sediment gets deposited or gets carried away. These deposits can be either on the banks of the stream or in-channel deposits, resulting in alterations in channel patterns. Detectable changes in channel patterns indicate important changes in both the watershed and the factors controlling morphology.

Researchers can use the evidence of channel changes, as prepared by a geomorphologist, as an indicator of the environmental health of the watershed.

Each channel type responds differently to changes in sediment supply or discharge. These responses can be of two types, including either vertical shifts (aggradation or degradation, as visible in the upward or downward position of the channel bed) and/or lateral shifts (sideways movement of the bed and banks, evident by old or abandoned channels on a floodplain).

Vertical Channel Shifts

The channel width-to-depth ratio keeps on changing along with the variation in the sediment load vis-à-vis transportation capacity. As there comes an increase in sediment supply beyond the transport capacity of the river, sediments tend to get deposited; this is referred to as aggradation. It leads to an increase in the width-to-depth ratio of the channel, and the level of channel stability decreases.

This is clearly visible in the aerial view of the river channel, where one can find an increase in the size and extent of sediment depositions within the channel over time. In cases where the sediment supply is less than the transportation capacity of the river, sediments are washed away, which results in the degradation of the channel.

Lateral Channel Movement

Displacement of the channel laterally across a valley flat surface also indicates variations in the conditions upstream. Lateral movement is often caused by either progressive bank erosion or channel avulsion. Progressive bank erosion is the result of sediment aggradation within the channel or can occur simply from natural meandering processes.

Whereas, unlike channel erosion, channel avulsion is usually a relatively sudden and major shift in the position of the channel to a new part of the floodplain (called as first- order avulsion), a sudden re-occupation of an old channel on the floodplain (known as a second-order avulsion), or a relatively minor switching of channels within a braided channel or other similarly active channels (third-order avulsion) (Nanson and Knighton, 1996).

Lateral channel movement influences the riparian zone (i.e., the interface between land and a river or stream), eroding some areas and building up others. The channel’s boundary conditions and the relationship between the stream and the valley through which it flows will determine the limit of lateral channel movement.

If no constraints are imposed, such as valley confinement, bridges, or dykes, and the valley flat is filled with erodible material, then the channel is usually capable of eroding across the entire extent of its floodplain.

Wherever valley width exceeds channel width, a potential for lateral channel movement exists. In confined systems where the valley is only marginally wider, the extent of lateral movement is limited.

In forested valleys, the additional bank strength provided by riparian vegetation can limit lateral channel movement and enable stable channel morphology to exist in an environment in which it otherwise may not occur.

Changes in the patterns of in-channel sediment storage in bars and islands are also an early indicator of future channel problems. Braided channels are amongst the most active of all the stream channels, characterized by rapid lateral migration rates and often undergoing net vertical aggradation.

Channel Morphology and Classification

Channel Morphology

Definition of Channel

Channel Structure