Basin Morphometry of Maingra River, district Gwalior ... · PDF filedrainage map of the basin was prepared with the help of Survey of India topographic sheets on ... (m.) 120 Relief

INTERNATIONAL JOURNAL OF GEOMATICS AND GEOSCIENCES

Volume 1, No 4, 2011

© Copyright 2010 All rights reserved Integrated Publishing services

Research article ISSN 0976 – 4380

891

Basin Morphometry of Maingra River, district Gwalior, Madhya Pradesh,

India Vineesha Singh, U.C.Singh

School of Studies in Earth Science, Jiwaji University, Gwalior (M.P.)

[email protected]

ABSTRACT

The term morphometery senses the measurements and analysis of form and its properties.In

context of geomorphology which is science of landforms it is concerned with the various

geometrical aspects of the landforms.Morphometric analysis of Maingra basin was carried .The

basin morphometric parameters such as linear and aerial aspects of the river basin were

determined and computed. The parameters considered for anaylisis are stream length, bifurcation

ratio, drainage density, stream frequency, Drainage texture, form factor circularity ratio,

elongation ratio, compactness ratio etc. The Maingra basin has a dendritic to parallel drainage

pattern. It is the 4th

order drainage basin. Logarithm of number of stream vs stream order and

length of stream segment vs stream order were computed in the basin area.

Keywords: Morphometry,Linear aspect,Aerial aspect,Relief aspect ,Basin analysis

1. Introduction

Geomorphometric analysis is the measurment of the three dimentional geometry of land forms

and has traditionally been applied to watershed, drainages,hill slopes, and other group of terrain

features (Barber,2005). Drainage basin or basins should be the study area for better

understanding of the hydrologic system. Basin morphometry is a means of numerically analyzing

or mathematically quantifying aspects of drainage channels. Spatial arrangement of streams have

given rise to a particular design which is called the drainage pattern. Morphometric analysis

requires measurement of linear features, gradient of channel network and contributory ground

slopes of the drainage basin (Nautiyal, 1994). The morphometric characteristics of various basins

have been studied by many scientists using conventional(Horton,1945, Strahler,1957) and

Remote sensing and GIS methods (Nag,1998;Srinivasa,2004;Chopraetal,2005;Nookaratram et al

2005;Thakkar et al.2007;Bhatt et al. 2007; Kar et al. 2009; Rao et al. 2010).

Remote sensing techniques using satellite images are convenient tools for morphometric analysis.

The satellite remote sensing has the ability to provide synoptic view of large area and is very

useful in analyzing drainage morphometry. The image interpretation techniques are less time

consuming than the ground surveys, which coupled with limited field checks yield valuable

results.

2. Study Area

The Maingra river is one of the main tributary of the Non river system, covers an area

285.081sq.km.The investigated area is enclosed between latitudes 250

55’ N and 260 5’ N and





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longitudes 780 5’ E 78

0 15’ E falling in the Survey of India(SOI) toposheet nos. 54 J/4 and K/1

on the 1:50,000 scale(fig 1). The river incorporated with sub river basins of Chinaur and Larma

nadi claims an area of 285.08167 km2

that falls under the Gwalior district.The study area falls in

the semi -arid region. The physiography of the study area varies from gentle sloping pediments

to gentle sloping alluvial plain. The area is well represented by denudational hills, alluvial plains,

flood plain, structural hill forming soil covers of clay with sand, kankar and alluvium. The area

falls under the sub tropical climate and temperature ranges from 30.6 max and 7.4 C min in the

December 44.5 C0 max and 23.0 C0 min. in the May. The average annual rainfall in the district is

1031.1 mm.(year 2008).

Figure 1: Location map of the study area

2.1 Data base and Methodology

For the purpose of the morphometric analysis of the basin under study, the base map and a

drainage map of the basin was prepared with the help of Survey of India topographic sheets on

1:50,000 scale(fig 2).The toposheets and digital data were geometrically rectified and

georeferenced to world space coordinate system using digital image processing software(ERDAS

Imagine 9.1).Digitization work has been carried out for entire analysis of basin morphometry

using the ERDAS Imagine 9.1 and Arc GIS software ver. 9.2.The orders were designated to

each stream following Strahler (1964) stream ordering technique. The stream number of various

orders were counted, while the stream length, basin length, basin area, and perimeter of the basin

were measured with the help of above software. The attributes were assigned to create the digital

data base for drainage layer of the river basin. The fundamental parameters namely stream length,

area, perimeter, number of stream, order and basin length were derived from the drainage layer.





893

The morphometric parameters for the delineated basin area were calculated based on formulas

suggested by various workers viz. Horton(1945),Strahler (1964),Schumn (1956),Miller(1953),

Nookaratnam(et al.2005).The various morphometric parameters such as linear aspect, aerial

aspect and relief aspect of the drainage network :Stream order(Nu),bifurcation ratio(Rb),stream

length(Lu),Mean stream length(Lsm),stream length ratio(RL),mean bifurcation

ratio(Rbm),Drainage density(D),stream frequency(Fs), drainage texture(Rt),elongation

ratio(Re),circularity ratio(Rc),form factor(Rf), lemniscate(k),compactness constant(Cc),constant

of channel maintenance(C),infiltration number(If),basin Relief (H),Relief ratio((Rh) were

computed.

3. Results and Discussion

In the present study, morphometric parameters of the Maingra basin were determined and their

results are summarized in Table 1.

Table1: Results of Morphometric analysis of study area, district Gwalior

Morphometric parameters Maingra Basin

Basin Area (A)

(sq. Km.) 285.08167

Total Number of Stream (Nu) 142

I 109

II 25

III 07

Streams

Order(u)

IV 01

I 95.57973

II 42.44254

III 79.4492

Stream Length(Lu)

(Km.)

IV 27.40035

Perimeter(P)

( Km.) 73.594389

Basin Length (Lb)

(Km.) 26.72646

Elongation Ratio (Re) 0.712

I 0.88

II 1.697

III 11.35

Mean stream length in Km (Lsm)

IV 27.40035

II/I 0.444

III/II 1.872

Stream Length Ratio

(RL)

IV/III 0.345

Texture Ratio (Rt) 1.929

Basin Relief(H)

(m.)

120

Relief Ratio (Rh)





894

I/II 4.36

II/III 3.57

Bifurcation Ratio (Rb)S

III/IV

07

Mean Bifurcation Ratio (Rbm) 4.92

Drainage density (D)

(Km./Km. 2) 0.859

Stream frequency(Fs) 0.498

Form factor(Rf) 0.399

Circulatory ratio(Rc) 0.661

Length of overland flow (Lg)

(Km.) 0.582

Lemniscate (k) 0.626

Compactness Constant(Cc) 1.229

Constant channel maintenance(C) 1.164

Infiltration Number(If) 0.42778

Linear Aspect

Stream Order (Nu)

In the drainage basin analysis the first step is to determine the stream orders and is based on a

hierarchic ranking of streams. In the present study, the stream segments of the drainage basin

have been ranked according to Strahlers stream ordering system.

Figure 2: Drainage Order map of the study area





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According to Strahler (1964),the smallest fingertip tributaries are designated as order 1,where

two first-order stream join, a channel segment of order 2 is formed ; where two segment of order

2 join, a segment of order 3 is formed ; and so on. The trunk stream through which all discharged

of water and sediment passes is therefore the stream segment of the highest order. The study area

belongs to the 4th

order drainage basin(fig2).The total number of 142 streams were identified out

of which 109 are I order,25 are II order,07 are III order,01 is indicating IV order stream.

Drainage pattern of the basin has been observed as mainly dendritic in the upper side of the

study area, which indicate the homogeneity in texture and lack of structural control, while the

some channels have been observed as parallel pattern in the lower side which indicate a gentle,

uniform slopes and with less resistant bed rock.

3.1 Stream Length (Lu)

The length of the stream channel is a dimensional property, which reveals the size of the

component of drainage lines. It is the total length of stream in a particular order. It is the most

significant hydrological feature of the basin as it reveals surface runoff characteristics. Stream of

relatively smaller length are characteristics of areas with larger slopes and finer texture.

Generally, the total length of the stream segment is maximum in first order streams and

decreases as the stream order increases. The numbers of stream of various orders in a basin were

counted and their lengths are measured with the help of the software. Relationship between

logarithm of number of streams versus stream order and logarithm of length of stream versus

stream order were measured(fig 3 and 4) and calculated in Table 2.Plot of logarithm of stream

length versus stream order (fig 5) showed the linear pattern which indicates the homogenous

rock material subjected to weathering erosion characteristics of the basin. Deviation from its

general behavior indicates that the terrain is characterized by variation in lithology and

topography.

Table 2: Relationship between Logarithm of Number of Streams versus Stream order and

Logarithm of Length of Stream versus Stream order

River

Basin

Stream

order

u

Number of

Streams Nu

Log Nu

(Number of

Stream)

Total Length of

Stream in Km.

Lu

Log Lu

(Stream

Length)

1

109 2.037426 95.57973 1.980366

2 25 1.39794

42.44254 1.627801

3

07 0.845098

79.44927

1.90009

Maingra

Basin

4

01

0 27.40035 1.437756





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Regression of number of stream segments versus stream

0rder

0

0.5

1

1.5

2

2.5

1 2 3 4 5 6

Stream Order,u

Lo

g(N

um

be

r o

f

Str

ea

m),

Nu

Figure 3: Relationship between Logarithm of Number of Streams versus Stream order

Regression of stream length versus stream order

0

0.5

1

1.5

2

2.5

1 2 3 4 5

Stream Order,u

Lo

g (

Str

eam

Len

gth

) ,L

u

Figure 4: Relationship between Logarithm of Length of Stream versus Stream order

3.2 Mean Stream Length (Lsm)

The mean length of a channel is a dimensional property and reveals the characteristic size of

drainage network components and its contributing basin surface (Strahlers, 1964).The mean

stream length (Lsm) have been calculated by dividing the total stream of order ‘u’ and number of

streams of segment of order “Nu’. Table 1 indicates that Lsm values of the basin is total

41.32735 respectively.

3.3 Stream Length Ratio(RL)





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Stream length ratio(RL) may be defined as the ratio of the mean length of the one order to the

next lower order of the stream segment(Table 1)Horton(1945).The RL between streams of

different orders in the study area reveals that there is a variation of RL in basin(Table 1).The

variation might be due to change in slope and topography.Chinaur and Larma sub- basins show

an increasing trend in length ratio from lower to higher order indicative their mature geographic

stage whereas in Maingra sub- basin ,there is a change from one order to another order indicating

its late youth stage of geomorphic development(Singh and Singh,1997).

3.4 Bifurcation Ratio (Rb)

The term bifurcation ratio(Rb) may be defined as the ratio of the number of stream segments of

the given order to the number of the segments of the next higher

order(Schumn,1956).Bifurcation ratios range between 3.0 to 5.0 for sub basins in which the

geologic structure do not distort the drainage pattern (Strahler,1964). Strahler (1957)

demonstrated that bifurcation ratios show a small range of variation for different regions or for

different environment except where the powerful geological control dominates. The higher

values of Rb indicates strong structural control in drainage pattern while the lower values are

indicative of not effected by structural disturbances. The mean bifurcation ratio (Rbm) is 4.92 for

the study area (Table 1),which indicates that geological structure are less disturbing the drainage

pattern.

3.5 Aerial aspect

Area (A) and perimeter (P) of the sub-basin are the important parameters in quantitative

morphology. Basin area is the hydrologically important because it directly affects the size of the

storm hydrograph and the magnitudes of peak and mean runoff. The aerial aspect of the drainage

sub-basin such as Drainage density (D), Stream frequency(Fs), Drainage Texture (Rt), Form

factor (Rf), Circularity ratio (Rc), Elongation ratio (Re), Length of overland flow (Lg),

Lemniscate (k), Compactness Constant(Cc), Constant channel maintenance(C), Infiltration

Number(If) were calculated and results have been given in Table 1.

3.6 Drainage density (D)

Drainage density(D) expresses the closeness of spacing of channels, thus providing a

quantitative measure of the average length of stream channel for the whole basin.The total length

of the stream of all orders divided by the area of the basin(Horton,1932). In general, the low

drainage density leads to coarse texture while high drainage density leads to fine texture (Strahler,

1964). High drainage density is the resultant of weak and impermeable subsurface material and

sparse vegetation and mountainous relief. The drainage density (D) of the basin is 0.859 km/

km2

respectively indicating low drainage density. It indicates that the basin is highly permeable

sub soil and sparse vegetation cover.

3.7 Stream frequency (Fs)

Stream frequency (Fs) is the total number of stream segments of all orders per unit area (Horton,

1932).The stream frequency of the basin is 0.498.The low value which indicates the sub-basin





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possesses low relief and the almost flat topography. Due to permeable rocks the surface runoff is

low and infiltration capacity is high within in the study area.

3.8 Drainage Texture (Rt)

Drainage texture is one of the important concept of geomorphology which means that the relative

spacing of drainage lines. Drainage texture is on the underlying lithology, infiltration capacity

and relief aspect of the terrain. Rt is total number of stream segments of all orders per perimeter

of that area (Horton, 1945). (Smith, 1950) has classified drainage texture into 5 different textures

i.e., very coarse (<2), coarse (2 to 4), moderate (4 to 6), fine (6 to 8) and very fine (>8).In the

present study, the drainage texture of the basin is 1.929 respectively. It indicates that category is

very coarse drainage texture.

3.9 Form factor(Rf)

According to Horton(1932) ,form factor may be defined as the ratio of basin area to square of

the basin length.The value of form factor would always be less than 0.754(for a perfectly circular

basin).Smaller the value of form factor, more elongated will be the basin. The basins with high

form factors have high peak flows of shorter duration, whereas elongated basin with low form

factor ranges from 0.399 indicating them to be elongated in shape and flow for longer duration.

3.10 Elongation ratio (Re)

Schumn, 1956 used an elongation ratio (Re) defined as the ratio of diameter of a circle of the

same area as the basin to the maximum basin length. The value of Re varies from 0(in highly

elongated shape) to unity i.e. 1.0(in the circular shape).Thus higher the value of elongation ratio

more circular shape of the basin and vice-versa. The circular basin is more efficient in run-off

discharge than an elongated basin (Singh and Singh, 1997).The value of elongation ratio

generally varies from 0.6 to 1.0 over a wide variety of climatic and geologic types. Values close

to 1.0 are typical of regions of very low relief, whereas that of 0.6 to 0.8 are usually associated

with high relief and steep ground slope (Strahler, 1964).These values can be grouped into 3

categories, namely circular (>0.9), oval (0.9 to 0.8) and less elongated (<0.7).The Re of the basin

of the study area 0.712 indicates basin to be elongated with high relief.

3.11 Circularity ratio (Rc)

It is the ratio of the area of the basin to the area of a circle having the same circumferences as the

perimeter of the basin(Miller,1953).The value of circularity ratio vary from 0(in a line) to 1.0(in

a circle).Higher the value of Rc more circular shape of the basin and vice-versa. The value of Rc

is influenced by length and frequency of streams, geological structure, landuse/land cover,

climate, relief and slope of the basin. In the present study, The Rc value is 0.661.It indicating

that the basin is elongated in shape ,low discharge of runoff and highly permeable of the sub soil

condition





899

3.12 Length of overland flow (Lg)

This term refers to the length of the runoff the rain water on the ground surface before it gets

concentrated into definite stream channels (Horton, 1945).This factor relates inversely to the

average slope of the channel and is quite synonymous with the length of sheet flow to a large

degrees. The length of overland flow (Lg) approximately equals to half of the reciprocal of

drainage density (Horton, 1945).Lengths of overland flow thus calculated for basin is 0.582

respectively (Table1).

3.13 Lemniscate (k)

Chorely et.al.(1957),express the lemniscate value to determine the slope of the basin. In the

formula k= Lb2/4*A where, Lb is the basin length (km) and A is the area of the basin (km

2). The

lemniscate (k) value for the basin is 0.626 respectively

3.14 Constant channel maintenance(C)

Schumn(1956)has used the reciprocal of drainage density as a property termed constant of

channel maintenance. It is expressed in sq km./km. Since it represents the drainage to maintain

one unit of channel length, hence it is a measure of basin erodibility. The values of basin are

1.164 respectively (Table 1), expressing strong lithologic rocks with a surface of high

permeability.

3.15 Infiltration Number (If)

Infiltration number is determined by multiplying the value of drainage density (D) and stream

frequency (Fs). It is expressed by formula If=D*Fs where, D is the Drainage density and Fs is

the stream frequency. Thus higher the value of infiltration number greater the permeability of

soil cover. In the present basin value are 0.42778 respectively (Table 1).

3.16 Relief aspect

The relief measurements like basin relief and relief ratio are calculated in Table 1.

3.17 Basin Relief (H)

The elevation difference the highest and lowest points of the valley floor of sub -basin is known

as the total relief of that sub-basin. The contour values varies from 220 m. to 360 m.in the study

area.

3.18 Relief ratio(Rh)

The relief ratio (Rh) of maximum relief to horizontal distance along the longest dimension of the

basin parallel to main stream is termed as relief ratio (Schumn, 1956 Table 1). According to him,

there is direct relationship between the relief and channel gradient. The Rh is normally is

increase with decreasing the drainage area and size of sub-basin of a given drainage





900

basin(Gottschalk,1964).The values of Rh are given in Table 1.It is observed that high values of

Rh indicate steep slope and high relief(360 m.) while low values may indicate the lower degree

of slope and small ridges.

4. Conclusions

The quantitative analysis of morphometric parameters is found to be of immense utility in river

basin evaluation, watershed prioritization for soil and water conservation, natural resource

management at micro level. The morphometric analysis of the drainage network of the Maingra

basin exhibits the dendritic(which indicates the homogeneity in texture and lack of structural

control) pattern, in some parts which represents to parallel pattern which indicate a gentle,

uniform slopes and with less resistant bed rock .The variation in stream length ratio might be due

to changes in slope and topography. The sub-basin is having low relief of the terrain and

elongated in shape. The low drainage density which indicates that the sub-basins is highly

permeable sub soil and sparse vegetation cover. Plot of logarithm of stream length versus stream

order (fig 3,4) showed the linear pattern which indicates the homogenous rock material subjected

to weathering erosion characteristics of the basin. Deviation from its general behavior indicates

that the terrain is characterized by variation in lithology and topography. The higher values of Rb

is indicates strong structural control drainage pattern while the lower values indicative of not

effected by structural disturbances. The mean bifurcation ratio (Rbm) are 4.92 for the study

area(Table 1),which indicates that geological structure are less disturbing the drainage pattern.

The drainage texture falls under the category of very coarse drainage texture (<2). The

Circularity ratio are 0.661 which indicating that the sub-basin is elongated in shape, low

discharge of runoff and highly permeable of the sub soil condition. The elongated basin with low

form factor ranges from 0.399 indicating them to be elongated in shape and flow for longer

duration.

Remote sensing and GIS have best efficient tool in drainage delineation and updation in the

future study.

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5. Guttschalk, L. C.1964, Reservoir sedimentation .In: V,T chow (ed.), Handbook of

applied hydrology ,McGraw Hill ,Book Company,Newyork,Sections. pp 4-11.

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Documents

Basin Morphometry of Maingra River, district Gwalior ... · PDF filedrainage map of the basin was prepared with the help of Survey of India topographic sheets on ... (m.) 120 Relief