Morphometric Analysis of River Basins

1 year ago

Atiqur Rahman

19 minutes

‘Morphometry’ means measuring the external form, and ‘Analysis’ means detail evaluation. Morphometric Analysis in Geomorphology means the detailed evaluation of landforms through mathematical measurement.

Mathematical or quantitative measurement helps us in analyzing the landforms accurately for any planning and development purposes. Morphometric Analysis is also very useful as it quantifies the landform features of evolutionary significance.

Morphometric Analysis of River Basins

Generally, River Basins are taken as units for Morphometric Analysis to understand geomorphic and hydrologic processes better. A river basin is defined as an area of land where surface water enters the area in any direction from any source, which converges to a single point before exiting the basin (Fig.). After exiting the basin, waters join another water body, such as a river, lake, sea, or ocean.

The River basins are a very important and ideal ecological unit for managing and planning natural resources, as there is only one outlet/ exit point for materials (soil and water) of the whole area. Morphometric Analysis of river basins is very useful for management and planning purposes as it provides accurate information through mathematical calculation.

The Morphometric Analysis of a river basin is done under the following three heads:

Linear Aspects: One dimension
Areal Aspects: Two dimensions
Relief Aspects: Three dimensions

Linear Aspects of Morphometric Analysis

1. Stream Order

In a river basin, a network of streams is distributed or arranged in a hierarchical order (Fig.). The networking starts from small fingertip channels draining into progressively larger channels downstream. Stream Order refers to the method of assigning designation to each stream in that hierarchical arrangement.

Stream order is the first step of measuring the landform characteristics of a river basin upon which most of the Mormpometric Analysis relies. Many eminent geomorphologists have developed different ways to array or designate streams in a river basin during the 20^th Century.

Strahler’s method is widely accepted and extensively used all over the world. According to him, the smallest fingertip tributaries are designated as 1st order streams. Where two 1st order streams join together, a 2nd order stream is formed; where two 2nd order streams join together, a 3rd order stream is formed; and so on. The highest-order stream exit the river basin, where all the lower-order streams converge to a single point.

While designating the order of streams in a river basin, one should remember the following points.

Do not follow the mathematical calculation.
When two of the same order streams come together, increase the number by one to designate the resultant stream.
When two streams of different order come together, take the number of the higher-order stream.

One will observe the following characteristics while moving from lower-order streams to higher-order streams:

The velocity of the water flow decreases
Width of the stream or volume of stream water increases
The temperature of stream water increases
Sediment load increases
Turbidity increases
Mineral nutrients increases
The rocky bottom becomes muddy/ sandy bottom

2. Stream Number

The total number of streams in each order is termed the Stream Number. After Stream Order, the 2nd step in Morphometric analysis is to count the Stream Number. The Stream Number decreases with the increasing order of the stream (Table). In other words, stream number is inversely proportional to stream order.

Horton has developed the ‘Law of Stream Number’. According to this Law, when Stream Number (taken in arithmetic scale)is plotted against Stream Order (taken in logarithmic scale), it gives a negative linear pattern (Fig.).

It means several streams from highest to lowest order in a particular basin tend to give a Geometric Series. A 6th-order river basin should be 1, 3, 9, 27, 71 and 213 in ideal condition. In the 4th-order river basin shown in Figure, the series is 1, 5, 14 and 62, which is plotted on the logarithmic scale to the right side of the Figure.

3. Bifurcation Ratio

The bifurcation Ratio is the ratio between the number of streams of any given order and the number of streams in the next higher order. It can be expressed in the following equation.

BR = Sn / Sn+1

Where

BR = Bifurcation Ratio

Sn = Total Number of streams in nth order

Sn+1 =Total Number of streams in n+1th order

We can calculate the Bifurcation Ratio between the number of streams in 1^st order and that of in 2^nd order; between the number of streams in 2^nd order and that of in 3^rd order and so on. The Mean Bifurcation Ratio is calculated by taking an average of all the bifurcation ratios of consecutive streams in the river basin.

The Bifurcation Ratio and Mean Bifurcation Ratio of the river basin shown in the Figure are calculated in the Table. The Mean Bifurcation Ratio of the river basin shown in the Figure is 4.07.

The Mean Bifurcation Ratio of a river basin says approximately how many times the number of stream segments increases when we move from higher to lower order. It is nothing but the constant of the Geometric Series explained under the heading Stream Number.

The bifurcation Ratio depends upon relief, rock type and dissection of rocks. In relatively homogeneous rock types, the value of the Mean Bifurcation Ratio of a river basin varies between 3 and 5. When any geological structure controls the drainage pattern, the Mean Bifurcation Ratio goes beyond 5. A value of 2 is rarely found. A value of 10 or more is possible in elongated basins with narrow, alternating outcrops of soft and resistant strata.

When the bifurcation ratio is low, there are high flooding possibilities as water accumulates rather than spreads out. Human intervention plays an important role in reducing the bifurcation ratio, which augments the risk of flooding within the basin.

In an area of uniform climate, rock type and history of geologic development, the Bifurcation Ratio tends to be constant from one order to the next. Hence that is the single ratio that characterizes the entire basin.

4. Stream Length

Stream Length is the total length of all the streams of a particular order, and Mean Stream Length is the average stream length of that order. As we have seen, the number of streams increases with the decrease in stream order, likewise, the total length of the streams increases with the decrease in stream order.

However, the mean stream length decreases with the decrease in stream order. Unlike the Bifurcation Ratio, the Stream Length Ratio is the ratio between the mean length of streams of a particular order and that of the next lower order. It can be expressed in the following equation.

SLR = Ln / Ln-1

Where

SLR = Stream Length Ratio

Ln = Mean Length of streams in nth order

Ln-1 = Mean Length of streams in n-1th order

Table: River Basin Characteristics of the River Basin Shown in Fig.

Stream Order	Stream Number	Bifurcation Ratio	Mean Stream Length (km.)	Stream Length Ratio	Average Basin Area (km²)	Average Channel Slope (tan θ)
1	62	4.43	.6	1.8	0.05	0.29
2	14	2.8	1.08	1.19	0.15	0.14
3	5	5	1.29	3.79	0.86	0.075
4	1		4.9		6.1	.03

Mean Bifurcation Ratio: 4.43+2.8+5/ 3 = 4.07

We can calculate the Stream Length Ratio between the mean length of all streams in the 4th order and that of in the 3rd order; between the mean length of all streams in the 3rd order and that of in the 2^nd order and so on (Table).

Like the Law of Stream Number, Horton has also developed ‘Law of Stream Length’. According to this Law, the Cumulative Mean Length of streams increases in geometrical progression with the increase in Stream Order. If stream order is taken on X-axis on an arithmetic scale and the cumulative mean length of streams on the Y-axis on a logarithmic scale, it gives a positive linear pattern. The relationship between Stream Length and Basin Order is very interesting which is as follows.

Stream Order Vs Cumulative Stream Length of Drainage Basin Shown in Figure Above

There is a negative relationship between Stream Order and Total Stream Length
There is a positive relationship between Stream Order and Mean Stream Length
There is a positive relationship between Stream Order and Cumulative Mean Stream Length. (Fig.) Besides, the latter increases geometrically with successive higher order.

5. Sinuosity Index

No river ever flows in a straight path. The Sinuosity Index explains how much a river deviates from the straight path. It is the ratio between the actual length of a stream and the length of the expected straight path of the stream.

It helps us to understand the effect of terrain characteristics on river flow. Many scholars have developed methods to calculate Sinuosity Index. Schumm’s method is widely used, which is expressed in the following equation.

SI = AL / EL

Where,

SI = Sinuosity Index

AL = Actual length of the stream

EL = Expected straight path of the stream

Based on the values, Schumm categorized five courses of the river. When it is 1, the course is straight; when it is more than 20, the course is torturous. In between, there are transitional, regular and irregular courses. Figure 4 shows the shape of all these types of streams. The Sinuosity Index of the main stream shown in Figure 4 is 1.17 (5.75 km. / 4.9 km.). It means the stream’s course is transitional, i.e., between straight and regular.

Areal Aspects of Morphometric Analysis

1. Basin Shape

The shape of the basins varies from place to place depending on relief, rock type, slope, geological structure etc. The ideal shape of a drainage basin resembles a pear. Streams descending from a mountainous zone to hilly or plateau regions generally have more elongated basins compared to those streams descending from hilly or plateau regions to the plains.

Assessment of a basin’s shape can be used to explain certain hydrological processes. There are various methods to assess the shape of basins. Schumm’s Elongation Ratio is very popular and is used widely which is expressed as follows.

ER = D / L

D = 2√A / √π

Where,

ER = Elongation Ratio

D = Diameter of the circle with the same area as the basin

L = Basin length

A = Area of the basin

Sinuosity Index, Basin Shape and Basin Area

The value of the Elongation Ratio varies from 0 to 1. The higher the value of the Elongation Ratio, the more circular the basin. The lower the value of the Elongation Ratio, the more elongated the basin. The basin area of the river basin shown in Figure 4 is 44.2 km2 and the basin length is 4.9 km.

After putting the values in the above equation, the Elongation Ratio is determined as 0.76. It shows the basin shape is more circular rather than elongated. The shape of the basin is ideal, i.e. pear shape.

2. Basin Area

Every stream/ river has a basin. The basin area of any stream having any stream order can be determined. Basin Area is the total area of a stream of a particular order and Mean Stream Area is the average stream area of that order. The area of the basins increases with the order. For example, the Basin Area of the 2nd order stream is the total area of all 1st order streams contributing to it plus the total inter-basin areas (as shown in Fig. 4).

According to the Law of Basin Area, developed by Strhaler, the mean basin areas of successive higher stream orders tend to form a geometric series beginning with a mean basin area of the 1st order basin. When Mean Basin Areas are plotted on a logarithmic scale of the vertical axis against the respective basin orders on the arithmetic scale of the horizontal axis, it produces a straight line.

The relationship between the Mean basin Area and Basin Order of the drainage basin (shown in Fig. 2) is shown in Fig. 5.

Stream Order Vs Mean Basin Area of Drainage Basin Shown in Figure 2

Like the Bifurcation Ratio and Stream Length Ratio, Basin Area Ratio is also determined. Basin area Ratio is the ratio between the mean area of the streams of any given order and the mean area of streams in the previous lower order. It can be expressed in the following equation:

BAR = An / An-1

Where,

BAR = Basin Area Ratio

An = Mean area of the stream of nth order

An-1= Mean area of the stream of n-1th order

We can calculate the Basin Area Ratio between streams of the 4^th order and 3^rd order; between the 3rd order and 2nd order; and between the 2^nd order and 1^st order.

3. Drainage Frequency

Drainage Frequency is defined as the total number of streams per unit area. The Drainage Frequency shows the dissection or the destruction of a relatively flat landscape through an incision and stream erosion.

Generally, most of the first-order and second-order streams of many regions are seasonal, i.e. they develop along the hill slopes during the rainy season due to torrential rain and become dry after the rainy season and look like gullies, the depth and width of which increase during the subsequent rainy season. The process is called dissection by which a land surface is cut up by eroding streams.

Thus, the uniformity of a surface is broken up by gullying and stream incision. Higher Drainage Frequency indicates lesser permeability and infiltration. Drainage Frequency depends on the variation in rock structure in the basin. Mature topography shows a lesser number of streams in comparison to younger topography.

The drainage basin is divided into small grid cells of equal area to determine Drainage Frequency. The streams are counted for each cell and then divided by the area of the cell. To show the spatial pattern of Drainage Frequency, the grid cell values are classified into 4/5 categories and a choropleth map is developed out of it (Fig. 6). The general categories of Drainage Frequency are: Very Poor, Poor, Moderate, High and Very High.

Drainage Frequency of Drainage Basin — Drainage Frequency of the Drainage Basin Shown in Figure 4

4. Drainage Density

Drainage Density is a very significant characteristic of a drainage basin because it influences the texture of a drainage system. Drainage density is influenced by geology, climate and the character of the terrain. For example, in humid climatic regions, high-relief areas have higher drainage density than the sub-humid region with lower-relief areas.

Density is also high on impermeable but easily erodible rocks, e.g. clay. Drainage Density also has an important influence on the area when there is a storm or cloud burst because water flow in channels is faster than overland flow. The risk of a fast flood decreases where the drainage density is high.

Drainage density is expressed as the ratio of the total length of all stream channels within a drainage basin to the total area of that basin. It can be derived as follows.

Dd = L1+ L2+ L3+L4………… LN / A

Where

Dd = Drainage Density

L1 = Length of stream No. 1

N = Total number of Nth streams

A = Total area of the basin

The DD of the given basin is .6 m/ km2. This figure does not show the spatial variation of Drainage Density within the basin. The drainage basin can be divided into small grid squares of equal area to know the spatial variation. The DD of each grid square is calculated, and based on the values, a choropleth map is prepared. (Fig. 7)

Drainage Density of Drainage Basin — Drainage Density of the Drainage Basin Shown in Figure 4

Relief Aspects of Morphometric Analysis

1. Stream Slope

Every stream flows on a slope. The velocity of water in a stream depends on the stream slope. A stream Slope is the ratio of a vertical drop of a stream to its horizontal distance. The vertical drop of a stream is determined by subtracting the absolute relief of the stream at its mouth from that of its origin.

The horizontal distance of the stream is determined by measuring the distance between the origin and mouth of the stream. The Mean Stream Slope of any stream order is the average slope of that order. The Stream Slope and Mean Stream slope are expressed in the following equation.

SS = V / H

Where,

SS = Stream Slope

V = Vertical drop

H = Horizontal distance

MSS = Summation of V nth order stream/ no nth order streams∕ Summation of H nth order stream/ no nth order streams.

Stream Order Vs Mean Stream Slope of Drainage Basin Shown in Figure 2

The Law of Stream Slope has been developed by Horton. According to the Law, Mean Stream Slope increases with decreasing stream orders in geometric series. It means when the Mean Stream Slope are plotted on a logarithmic scale of the vertical axis against the respective basin orders on an arithmetic scale of the horizontal axis, it produces a straight line of negative relation (Fig. 8).

2. River Profile

The river Profile is an outline of the course of the river as seen in a vertical section. The profiles of a river can be shown in two ways- a) along the river, and b) across the river. The profile along the river is called Long Profile and the profile across the river is called Cross Profile.

To show the Long/ Longitudinal Profile, a graph of distance versus elevation along the river is prepared(Fig. 9). It shows changes in the altitude of the course of a river from its source to its mouth. It is usually concave and the slope becomes gentler towards the mouth of the river. The profile of a river which has been gone through rejuvenation, shows numerous pronounced breaks indicating nick points or heads of rejuvenation.

To show the Cross Profile, a graph of distance versus elevation across the river is prepared (Fig. 10). Cross profile can be drawn at various stages of the river. The upper course of the river is generally ‘V-shaped’. The shape of the Cross Profile changes with the advancement of river. Both Longitudinal Profile and Cross Profiles at various parts of the river tell us about underlying materials as well as give insights into geologic processes and the geomorphic history of an area.

Longitudinal Profile of River

Cross Profiles at Various Stages of River

3. Area-Height analysis

Area-Height analysis of a river basin shows the measurement and analysis of the relationship between altitude and basin area to understand the degree of dissection and stage of erosion. The Area-Height analysis is popularly known as Hypsometric analysis. Hypsometric curves are drawn on graph paper to determine the area and height relationship.

There are usually two methods to draw a hypsometric curve in a river basin. In 1st method, the values of contours are plotted against the percentage of surface area above that contour in a river basin (Fig.11). The more mature the river, the more the hypsometric curve is more concave. By drawing a Hypsometric curve by this method, we can compare one part of a river basin that is more or less eroded in comparison to other parts.

In the 2^nd method, the relative height (h/H) is taken on Y-axis and the relative area (a/A) is taken on X-axis. Here ‘h’ is obtained by subtracting a specific contour’s value from the basin’s height. ‘H’ is the height of the basin; ‘a’ is the area above a specific contour; ‘ A’ is the river basin’s total area (Fig. 12).

The different shapes of the curve show the different stages of the river, i.e. Youth, Mature and Old. We can compare stages of denudation of two different river basins by applying this method.

Mathematical or quantitative analysis of the earth’s external features is called Morphometric Analysis. Morphometric Analysis of river basins is explained due to two reasons:

a) It is easy to understand the technique (Morphometric Analysis technique) through river basins;

b) The Morphometric Analysis of the river basin as a unit is very useful for planning purposes as the river basin is the ideal ecological unit.

Twelve important parameters of morphometry are explained under linear, areal and relief aspects. The measurement and calculation of these parameters, along with the significance of their values, are explained with suitable examples.

Morphometric Analysis of River Basins

Morphometric Analysis of River Basins