Drainage Basin Morphometry

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1 CHAPTER 5 Drainage Basin Morphometry 5.1 Introduction Morphometric analysis is refers as the quantitative evaluation of form characteristics of the earth surface and any landform unit. This is the most common technique in basin analysis, as morphometry form an ideal areal unit for interpretation and analysis of fluvially originated landforms where they exhibits and example of open systems of operation. The composition of the stream system of a drainage basin in expressed quantitatively with stream order, drainage density, bifurcation ration and stream length ratio (Horton, 1945). It incorporates quantitative study of the various components such as, stream segments, basin length, basin parameters, basin area, altitude, volume, slope, profiles of the land which indicates the nature of development of the basin. This modern approach of quantitative analysis of drainage basin morphology was given inputs by Horton (1945) the first pioneer in this field. Horton's law of stream lengths suggested that a geometric relationship existed between the numbers of stream segments in successive stream orders. The law of basin areas indicated that the mean basin area of successive ordered streams formed a linear relationship when graphed. Horton s laws were subsequently modified and developed by several geomorphologist, most notably by Strahler (1952, 1957, 1958, and 1964), Schumm (1956), Morisawa (1957, 1958), Scheidegger (1965), Shreve (1967), Gregory (1966, 1968), Gregory and Walling (1973). Subsequently a number of books by Bloom (2002), Keller and Pinter (1996) have further propagate the Morphometric analysis. Stream profile analysis and stream gradient index by Hack (1973) is another milestone in morphometric analysis. Many workers have used the principles developed by these pioneers to quantitatively study the drainage basin as a tool for landscape analysis (Sharma, 1987, Raj et. al., 1999, Awasthi and Prakash, 2001, Phukon, 2001, Sinha- Roy 2002). 115

2 Quantitative measurements of morphometry used as a reconnaissance tools to make inferences about particular characteristic of an area viz., tectonic activity. Some geomorphic indices like hypsometric integral, drainage basin asymmetry, stream length gradient index, mountain front sinuosity etch are used a measure of active tectonics (Keller and Pinter, 1996; Sinha-Roy, 2002). Landforms are created via erosional and depositional processes, the geometry of which is controlled by the processes that shape them. Morphometric analyses require measurement of linear features, gradient of channel network and contributing ground slopes of the drainage basin (Nautiyal, 1994). The morphometric analysis for individual sub basins has been achieved through measurements of linear, aerial and relief aspect of the basin and slope contribution (Nag and Chakraborty, 2003). The basin geomorphic characteristics have long been believed to be important indices of surface processes. These parameters have been used in various studies of geomorphology and surface-water hydrology, such as flood characteristics, sediment yield, and evolution of basin morphology (Jolly, 1982; Ogunkoya et al., 1984; Aryadike and Phil-Eze, 1989; Breinlinger et al., 1993; Jensen, 1991). By including basin characteristics such as elevation and main channel gradient, predictions of stream discharge were substantially improved in comparison to using only drainage area and precipitation (McArthur and Hope, 1993). More recently, terrain characterization became an important part in modelling surface processes (Nogami, 1995). The detailed analysis of morphometric and morphological character indicate the role of the neotectonics in shaping the drainage basin (Raj et.al., 1999). Geographical Information system (GIS) and Remote sensing techniques using satellite images are used as a convenient tool for Morphometric analysis. Many workers have carried out morphometric analysis using these new techniques. Digital Elevation Model (DEM) and Shuttle Radar Topography Mission (SRTM) widely used in drainage basin analysis. Srivastava, 1997, Nag, 1998, Duarah et al., 2011, carried out morphometric analysis, while Nag and Chakraborty (2003) deciphered the influence of rock types and structures in the development of drainage network in hard rock area. 116

3 As the main objectives of this work was to discover holistic stream properties from the measurement of various stream attributes, detailed morphometric analysis is carried out for the 41 fifth-order drainage sub-basins of Jia Bharali River catchment and discusses their feature and characteristic and also attempt to find out the stages of geomorphic development with the help of different morphometric parameter viz., streams order, streams number, streams length, mean streams length, bifurcation ratios, elongation factor, circularity index, shape factor, drainage density, stream frequency, texture ratio, relief ratio, length of overland flow, constant channel maintenance, infiltration number, hypsometric curve and longitudinal profiles. Morphological Studies of rivers are very important to study the behaviour of a river, its aggradations/degradation, shifting of the river course, erosion of river bank etc. and to plan remedial measure for erosion and other related problems. Most of the streams appear to be in conformity with the geological and structural setup of the area. For detail morphometric analysis of the drainage within Jia Bharali River catchment at first the fifth order sub basins are delineated from the available toposheet after assigning stream order to all the segments following Horton's (1945) method modified by Strahler s (1952). In general the entire fifth order sub basins are selected for the morphometric analysis in following heads: Linear Aspects : one dimension Areal Aspects : two dimensions Relief Aspects : three dimensions The prime objective of morphometric analysis is to find out the drainage characteristic to explain the overall evaluation of the basin. Morphometric analysis comprises a series of sequential steps. The drainage layer has been converted to digital format through on-screen digitization from available Survey of India (SoI) topographic maps using GIS software Arc-Info 9.1, in the scale of 1:50000 and the attributes were assigned to create the digital database. Toposheet for the total basin catchment is not available as the area has sensitive political controversy. Some part of the basin fall in the international boundary of Bhutan and China. All measurements were directly computed from the vector data that extracted from the topographic maps. The entire drainage segments were digitized as lines separately for each order (Strahler 1952). 117

4 Fifth order drainage sub-basins are delineated following surface water divide. Topological polygons were created and the attribute Table generated thus yielded the basinal areas. In absence of the Survey of India topographic maps for the northernmost part of the Jia Bharali basin, the surface water divide and was delineated with the help of satellite imagery and SRTM DEM. Major sub basin boundaries were also delineated following this method. Thus 41 fifth-order drainage basins were used as a statistical sample representative for the entire drainage system to compute the morphometric parameters analysis (Figure 5.1, Table 5.1). Figure 5.1: Delineated fifth order sub-basins for morphometric analysis The morphometric parameters for each basin were directly computed from the vector data extracted from the topographic maps (basic parameters). The data in the first category includes maximum order of the streams, number of streams in each order, length, area, perimeter, relief for each of the basins. Those of the second category are 118

5 the bifurcation ratios, elongation factor, circularity index, shape factor, drainage density, stream frequency, texture ratio, relief ratio, length of overland flow, constant channel maintenance and infiltration number. Linear, aerial and relief aspects of the basin were computed in GIS environment followed by simple linear regression analysis to see the mutual dependency of some variables viz., i) stream order vs. stream number, ii) stream order vs. stream length and iii) stream order vs. Mean stream length. For hypsometric analysis the elevation contour are generated in ArcInfo 9.1 from the SRTM DEM. The contour layer and the basin boundary are merged in a single layer and converted into polygon. From the attribute Table of this polygon layer the area the between two contours within the basin are noted. Maximum height (H) is the difference between the maximum elevation and the minimum elevation and, which are calculated by extrapolation. Mean elevation for each basin also calculated by dividing the sum of frequency of each pixel elevation by the total number of pixel in the basin. Details of the morphometric parameters are tabulated followed by analysis of the parameters through bivariate plots. 119

6 Table 5.1: Fifth order sub basin index and basin name used in the study Basin Index Basin Name Basin Perimeter (km) Basin Area (Sq km) 1 Dipota Nadi Jorasar Nadi Mansari Nadi Dibru Nadi Khari Dikrai Nadi Upar Dikrai Nadi Daigurang Nadi Khaina Nadi Lengtey Nadi Diju Nadi Pakke River Tributary of Pakke River Tributary of Kameng River Pasa Nadi Pani Nadi Papu River Chakrasong Nadi Tributary of Pacha River Pacha River Lengpla Nadi Phuchao Nadi Kade Nala Pakoti Nadi Hoda Nadi Huduri Nadi Kaun or Hukubu Nala Gayang River Ki Nala Miao Nadi Upstream of Dinang Bru Dibri Bru Difya River Khenda Nadi Taamchin RI (Sashi Chu) Meni Nadi Nimsinggoto River Dublo Kho Tribtary of Tenga River Dogong Kho Sessa Nadi Tipi Nala

7 All the fifth order sub basins are grouped into three divisions. The group of the completed fifth order drainage sub basin (Figure 5.2) are based on the lithotectonic setup of the area. The basins in Zone-I are predominantly within the alluvium south of HFT. Zone-II is mainly characterised by the folded Cenozoic/Gondwana sequence with pertinacious E-W structural lineament spreading into both side of MBT but within the HFT and the Pronounced NE-SW lineament. The Zone-III is characterised by dissected crystalline terrain. Figure 5.2: Showing the assign three Zone for the drainage basin 5.2 Linear aspects The drainage network transport water and the sediments of a basin through a single outlet, which is marked as the maximum order of the basin and conventionally the highest order stream available in the basin considered as the order of the basin. The size of rivers and basins varies greatly with the order of the basin. Ordering of streams is the first stage of basin analysis. 121

8 Stream Order (U) There are four different system of ordering streams that are available Gravelius (1914), Horton (1945), Strahler (1952) and Schideggar (1970). Strahler s system, which is a slightly modified of Hortons system, has been followed because of its simplicity. Where the smallest, unbranched fingertip streams are designated as 1st order, the confluence of two 1st order channels give a channel segments of 2nd order, two 2nd order streams join to form a segment of 3rd order and so on. When two channel of different order join then the higher order is maintained. The trunk stream is the stream segment of highest order. The total Jia Bharali drainage basin boundary and major river system are delineated from the satellite imagery and SRTM. It is found that Jia Bharali River is an 8th order stream. The analyses of morphometric parameters are carried out for the entire 41 fifth order basin. Stream Number (Nu) The total number of stream segments present in each order is the stream number (Nu). Nu is number of streams of order u. In this present study all the 5th basin are counted and tabulated for the analysis from the attribute Table of the vector layer (appendix- III). The total number of stream segments is found to decrease as the stream order increases in all the sub basins. The study reveals that the development of 1st order streams is maximum in the Himalayan dissected zones and minimum in the alluvial plains (Table. 5.2). Similarly the numbers of 2nd and 3rd order streams are gradually high from alluvial to highly dissected hills from south to north. Stream Length (Lu) The total length of individual stream segments of each order is the stream length of that order. Stream length measures the average (or mean) length of a stream in each orders, and is calculated by dividing the total length of all streams in a particular order by the number of streams in that order. The stream length in each order increases exponentially with increasing stream order. 122

9 From the overall drainage of the study area shows the frequency of the drainage development is less in the alluvial part (0.7 km -2 ) and high above the MBT (4.5 km -2 ) whereas the overall drainage frequency is 3.8 km -2. It reflects the frequency of the drainage is high in the upper part of MBT. The drainage density also shows that the development of drainage is higher in the upper part of MBT. The alluvial part has a drainage density of ~1 km -1 where as the area above the MBT is 2.9 km -1. The overall drainage density of the area is 2.6 km -1. It clearly reflects that the drainage development in the upper part of the MBT is high and the area is highly dissected. Mean Stream Length (Lū) Mean stream length of a stream channel segment of order u is a dimensional property revealing the characteristic size of components of a drainage network and its contributing basin surface (Strahler, 1964). The lengths of stream segments of up to 5th order are measured and the total length as well as Mean Stream Length (Lū) of each order is computed (appendix-iii). The mean stream lengths of stream increase with the increase of the order. But in some basin shows opposite relation, higher order stream has a small mean length. In Zone-I, Basin 2, in Zone-II, Basin 4, 12, 13, 16 and in Zone-III, Basin 18, 24, 29, 33, 35 the length of 5 th orders stream is extremely short. These basin shows variable lithology with asymmetry in nature and these basins are found along the major structural lineament. The basins shows high hypsometric integral value and high relative upliftment, reveals the tectonic control on these sub basins. In order to find the relation between basin area and the total stream length for respective sub basins a regression line is constructed using a double log graph. It is observed that the drainage area bears a power function relationship with stream length (Figure 5.3) 123

10 Figure 5.3 Log-Log plot of Basin Area (Au) vs. Total Stream Length (Lu) shows conformable relation of basin area and total stream length. Stream Length Ratio (RL) The Length Ratio (RL), which is the ratio of the mean length of the stream of a given order (Lu 1 ) to the mean length of the streams of the next lower order (Lu -1 ), is then calculated for each pair of the orders. Length ratio is for 1 st -2 nd and 2 nd -3 rd order of the alluvial plain basin are higher than the basin of other two zones. Elongated basins (Basin index 7, 14, 37, 41) shows high length ration (up to 14.1 in case of Basin41) in the higher order where as the basin (Basin index 12, 13, 16, 29, 35) with comparatively high circularity ratio shows the low length ratio (<1). The variation in length ratio, attributed to variation in slope of topography indicate youth stage of geomorphic development in the streams of the study area (Singh and Singh, 1997, Vittala et al., 2004) 124

11 Table 5.2: Summary of drainage basin parameters in the study area Division Order Stream Number Bifurcation Ratio Mean Bifurcation Ratio Stream Length (km) Mean Stream Length (km) Area (sq km) Drainage Density (km -1 ) Drainage Frequency (km -2 ) u Nu Lu Lū Au Dd Df South of HFT Nu=736 Lu= HFT-MBT Nu=4257 Lu= MBT-MCT Nu=20006 Lu= Above MCT Nu=287 Lu=179.5 In total (available drainage) Nu=25050 Lu=

12 Order Basin Index Order Table 5.3: Mean Stream Length for all the order for entire 41 fifth order basin Mean Stream Length Basin Index Mean Stream Length Order Ratio Basin Index Table 5.4: Stream Length Ratio for different order of the entire 41 fifth order basin Length Ratio (RL) nd/1st rd/2nd th/3rd th/4th Order Ratio Basin Index Length Ratio (RL) nd/1st rd/2nd th/3rd th/4th

13 Bifurcation Ratio (Rb) The bifurcation ratio is the ratio between the number of streams in one order and in the next. It is calculated by dividing the number of streams in the lower by the number in the higher of the two orders; the bifurcation ration of large basins is generally the average of the bifurcation rations of the stream orders within it. The bifurcation ratio of the basin of alluvial region is comparatively low than the Himalayan zone. The bifurcation ratio is range of 3-5 in case of overall drainage system of the basin. It is seen that the bifurcation ratio of 2nd and 3rd order stream is higher than the other ratio (Appendix-III and Table 5.2). The sub basins belongs to the Zone-I shows the bifurcation ratio of 2-4 of different order whereas the mean bifurcation ratio in between Similarly the Zone-II basins of eastern part of the Kameng River having origin along the MBT with N-S directional flow and basins origin in the extreme eastern boundary with a E-W flow have a mean bifurcation ratio of The bifurcation ratio of the lower order shows a higher value. This reflects the high dissection in the upland area. The sub basin 11 and 14 shows a high bifurcation ratio 4-8 in the higher order. The sub basin 11, Pakke river has an elongated course, it origin near the eastern margin of the basin and the trunk channel flows along the major structural control of MBT in the Gondwana sequence in E-W direction. It turns south in through a transverse lineament, flow across the MBT and it again turns towards east upto the MBT. It again turns to south along N-S transverse lineament and through Siwalik it confluence with Dibru N and flow as Bor Dikrai River up to Jia Bharali in the alluvium. The pattern of the river itself reflects the structural disturbance of the area. The higher Bifurcation ratio suggests that the area is tectonically active (Som et.al., 1998). In case of Pasa Nadi (basin index 14) shows higher bifurcation ratio of 6, this indicates the structural control. In longitudinal profile also it is also seen that in the river course there is lithological and structural control. And the drainage between the MBT and MCT have comparatively higher bifurcation ratio. As per the Horton (1945) bifurcation ratio having a less value about 2 to 3 is of flat region. The basins of alluvial plain the ratio higher order is approximately 2 it reflects that the lower part of the basin is flat. The mean bifurcation ratio is 3.8. Other hand the ration of the lower order is high and as per Horton these streams or of highly dissected drainage basins. 127

14 The Bifurcation Ratio is of fundamental importance in drainage basin analysis as it is the foremost parameter to link the hydrological regime of a watershed under topological and climatic conditions (Raj et. al., 1999). It helps to have an idea about the shape of the basin as well as in deciphering the run off behavior. The bifurcation ratio will not be exactly same from one order to the next order because of possibility of the changes in the watershed geometry and lithology but will tend to be consistent throughout the series. From the Figure 5.4- i,ii,iii, it is clear that the Zone-III basins have ruggedness topography as it shows a high variation in the bifurcation ratio. The Zone-II basins are also comparatively highly rugged topography than the alluvial part basins. The area under the Zone-II and Zone-III are moderately and highly dissected area and the drainage development is high. Mean Bifurcation Ratio ( Rb ) is calculated as the Arithmetic Mean Bifurcation Ratio and the result is tabulated corresponding to Sub-order basins as shown in the Table appendix-iii. Using Strahler's (1957) method of taking into consideration of actual number of streams that are involved in the ratio, Mean Bifurcation Ratio of different sub-basins was calculated. The mean bifurcation ratio is in between The basin having index 18 has the lower bifurcation ratio of 3 and the basin 11 has the higher bifurcation ratio of 5.9. The higher bifurcation ratio indicates there may be some structural distortion in that basin area. The overall plotting of the mean bifurcation ratio against the basin area it is seen that higher is the bifurcation ratio as the basin area increases. 128

15 a b Figure 5.4: a,b,c, are the plotting of bifurcation ratio and stream order of different basin in the Zone-I, Zone-II, Zone-III c a b Figure 5.5: a. shows the variation of mean bifurcation ratio. B. shows the trend of mean bifurcation ratio against basin area 129

16 Basin length (Lb): Basin length is the longest dimension of a basin to its principal drainage channel. Sub basin having index 1, 11 has the longest basin length of 33.9 km and 32.5 km accordingly and the sub basin 20 has the shortest basin length of 5.5km. Basin length and the basin area of the alluvial river are maximum and in the dissected hill it is minimum. Basin lengths for the entire basin are tabulated in the given appendix-iii. Regression Analysis Graphical presentation of i) the stream order and the stream number ii) the stream order and the stream length iii) the stream order and the mean stream length is prepared in a semi-log plot as suggested by Strahler (1957). For this regression analysis number of streams (Nu) of each order and their length (Lu) are noted from the attribute Table. All these aspects are then entered in an excel sheet and then the bifurcation ratio (Rb) is calculated. For graphical plot of Stream order Vs Stream number and Stream order Vs Stream Length we used the Regression Equation, which is y= a + bx (1) Where b is the co-efficient of the Regression equation, which can be calculated from the following formula ΣxΣy Σxy = n 2 ( Σx) Σx n b 2 Again the value of a can be calculated from a = y bx Where, y =Mean of y x = Mean of x By plotting the values of x, a and b in the regression equation (1), we get the value of y for corresponding stream number and stream length. Plotting the antilog values of y in the Y axis in logarithmic scale against x value (order) in the X axis in arithmetic scale, the three necessary bivariate plots are made. 130

17 Stream order vs. the stream number Graphical presentation (Figure 5.6, 5.7 and 5.8) of the total stream length against the stream order can also be prepared in a semi-log plot as suggested by Strahler (1957). It is observed that the number of stream segment increases with decreasing stream order in the entire sub basins i.e. negative regression relation. Figure 5.6 Stream order Vs Stream number (-ve corrlation) for the Zone-I Figure 5.7 Stream order Vs Stream number (-ve corrlation) for the Zone-II Figure 5.8 Stream order Vs Stream number (-ve corrlation) for the Zone-III 131

18 Table 5.5 Showing the Regression equation for Stream order vs. Stream Number Basin Index Regression Equation Basin Index Regression Equation 1 y= x 21 y= x 2 y= x 22 y= x 3 y= x 23 y= x 4 y= x 24 y= x 5 y= x 25 y= x 6 y= x 26 y= x 7 y= x 27 y= x 8 y= x 28 y= x 9 y= x 29 y= x 10 y= x 30 y= x 11 y= x 31 y= x 12 y= x 32 y= x 13 y= x 33 y= x 14 y= x 34 y= x 15 y= x 35 y= x 16 y= x 36 y= x 17 y= x 37 y= x 18 y= x 38 y= x 19 y= x 39 y= x 20 y= x 40 y= x 41 y= x Stream order vs. the stream length Generally, the total length of stream segments decreases with stream order. Graphical representation of the total stream length against stream order was also prepared in a semi-log plot as suggested by Strahler (1957). The general logarithms of the number of stream of a given order, when plotted against the order, the points lie on a straight line (Horton, 1945). Bivariate plot (Figure 5.9, 5.10 and 5.11) between stream order and total stream length shows negative exponential functions, indicating that the total stream length decreases with increase in stream order indicating that development of drainage is higher for the lower order. 132

19 Figure 5.9: Stream order Vs Stream Length (-ve corrlation) for the Zone-I Figure 5.10 Stream order Vs Stream Length (-ve corrlation) for the Zone-II Figure 5.11 Stream order Vs Stream Length (-ve corrlation) for the Zone-III 133

20 Table 5.6 Showing the Regression equation for Stream order vs. Stream length Basin Index Regression Equation Basin Index Regression Equation 1 y= x 21 y= x 2 y= x 22 y= x 3 y= x 23 y= x 4 y= x 24 y= x 5 y= x 25 y= x 6 y= x 26 y= x 7 y= x 27 y= x 8 y= x 28 y= x 9 y= x 29 y= x 10 y= x 30 y= x 11 y= x 31 y= x 12 y= x 32 y= x 13 y= x 33 y= x 14 y= x 34 y= x 15 y= x 35 y= x 16 y= x 36 y= x 17 y= x 37 y= x 18 y= x 38 y= x 19 y= x 39 y= x 20 y= x 40 y= x 41 y= x Stream order and the Mean stream length The values of mean stream length are plotted against respective stream order (Figure 5.12, 5.13, 5.14). These shows the positive relationship between mean stream length and the stream order for each drainage basin. Sub-basin with index 18 shows a relationship that reveals more or less a straight line regression of negative relation. Again in some basin it is observed an exception where the mean stream length of fourth order is much higher than that of the fifth order (basin index 2, 4, 12, 13, 16, 18, 24, 29 33, 35). Deviation from its general behaviour may suggest that the terrain is characterized by high relief and/or moderately steep slopes, underlain the various lithology and probable uplift across the basin (Singh and Singh 1997, Vittala et al., 2004). 134

21 Figure 5.12 Mean stream length vs. Stream order plotting of Zone-I Figure5.13 Mean stream length vs. Stream order plotting of Zone-II Figure 5.14 Mean stream length vs. Stream order plotting Zone-III 135

22 Table 5.7 Showing the Regression equation for Stream order vs. Mean Stream Length Basin Index Regression Equation Basin Index Regression Equation 1 y= x 21 y= x 2 y= x 22 y= x 3 y= x 23 y= x 4 y= x 24 y= x 5 y= x 25 y= x 6 y= x 26 y= x 7 y= x 27 y= x 8 y= x 28 y= x 9 y= x 29 y= x 10 y= x 30 y= x 11 y= x 31 y= x 12 y= x 32 y= x 13 y= x 33 y= x 14 y= x 34 y= x 15 y= x 35 y= x 16 y= x 36 y= x 17 y= x 37 y= x 18 y= x 38 y= x 19 y= x 39 y= x 20 y= x 40 y= x 41 y= x 5.3 Areal Aspect The areal aspect is the two dimensional properties of a basin. It is possible to delineate the area of the basin which contributes water to each stream segment. The watershed can be traced from where the stream has its confluence with the higher order stream along hillcrests to pass upslope of the source and return to the junction. This line separates slopes which feed water towards the streams from those which drain in to other streams. The information of hydrologic importance on fluvial morphometry is derived by the relationship of stream discharge to the area of watershed. The planimetric parameters directly affect the size of the storm hydrograph and magnitudes of peck and mean runoff is the basin area. The maximum flood discharge per unit area is inversely related to the size of the basin (More, 1967) 136

23 Drainage Area (Au) The entire area drained by a stream or system of streams such that all streams flow originating in the area is discharged through a single outlet is termed as the Drainage Area. Drainage area measures the average drainage area of streams in each order; it increases exponentially with increasing order. The total catchment area of Jia Bharali as well as for the 41 fifth order basin was computed from the topological polygon that are created by delineation basin from the toposheet following the surface water divide in ArcInfo9.1 The basin with index 1, i.e., Diputa River in Zone-I has a 255 sq km of basin area, Pakke River, with basin index 11, has the highest basin area of 328 sq km in Zone-II, which is the biggest basin among the 41 basin. In Zone-III, Dublo kho, basin index 37 has the highest basin area of 163 sq km. Relation between Basin area and Basin length It is seen area of the basins of alluvial area are maximum than that of other structural or transitional piedmont zone. In general the basin area and the basin length both are proportional and they shows almost +ve relation. This reflects that basin area is maximum when the basin length has a high value. Figure 5.15: Showing the relationship between Basin Area and Basin Length 137

24 Drainage Density (Dd) Drainage density has long been recognised as topographic characteristic of fundamental significance. This arise from that fact that drainage density is sensitive parameter which in many ways provides the link between the form attributes of the basin and the processes operating along stream course (Gregory and Welling, 1973). It reflects the landuse and affects infiltration and the basin response time between precipitation and discharge. It is also of geomorphological interest particularly for the development of slopes. Drainage basin with high Dd indicates that a large proportion of the precipitation runs off. On the other hand, a low drainage density indicates the most rainfall infiltrates the ground and few channels are required to carry the runoff (Roger, 1971). Dd is considered to be an important index; it is expresses as the ratio of the total sum of all channel segments within a basin to the basin area i.e., the length of streams per unit of drainage density. It is a dimension inverse of length (Horton, 1932). Dd is a measure of the texture of the network, and indicates the balance between the erosive power of overland flow and the resistance of surface soils and rocks. The factors affecting drainage density include geology and density of vegetation. The vegetation density influenced drainage density by binding the surface layer and slows down the rate of overland flow, and stores some of the water for short periods of time. The effect of lithology on drainage density is marked. Permeable rocks with a high infiltration rate reduce overland flow, and consequently drainage density is low. The drainage density is found to increase from south to north of the basin (Figure 5.16). In the south of HFT the drainage density is low about 1.0 km 1 (Table 5.2). Again it increases to about 2.9 km 1 between HFT and MBT followed by 3.0 km 1 between MBT and MCT. And the highest value of 3.6 km 1 attain in the area north of MCT. The drainage density for individual basin also shows conformable relation. The sub basin having index 1, Diputa Nadi has the lower density of 1.7km 1 in the alluvial part. The Basin no.35, Meni Nadi, tributary of Bichom river north of MBT shows the higher density of about 3.9 km 1 (Table 5.8). As per the zonation of basins, in this study on the basis of lithotectonic setup of the area, it is observed that the basins of alluvial part of Zone-I shows low drainage density ( km 1 ) as this area has a in 138

25 high permeability. The basins of Zone-II, shows comparatively higher value ( km 1 ). In the piedmont zone basins shows moderate drainage density. The precipitation in this area is very high whereas this area exhibit high vegetation also. From the Table 5.2 and the Table 5.8 it is observed that the Dd north of MBT is 3.0 km 1 confined with Bomdila Group of rock. The sub basins in the western part of the Jia Bharali catchment shows comparatively high drainage density ( km 1 ) than the eastern part ( km 1 ), which suggest the western part is highly dissected with a impermeable but erodible lithology. Figure 5.16 Drainage density map of the study area. Drainage density increases from south to north with higher value in the western part of the basin. 139

26 Drainage (Stream) Frequency (Fs) Drainage frequency may be directly related to the lithological characteristics. The number of stream segments per unit area is termed Stream Frequency or Channel Frequency or Drainage Frequency (Fs) Horton (1945). Table 5.2 reflects the total drainage frequency of the basins is 3.8 km -2 and the drainage frequency increase from south to north. In the alluvial part, south of HFT is 0.7 km -2 and increase abruptly 3.7 km -2 in between HFT and MBT again north of MBT in 4.5 km -2. The drainage frequency of the entire sub basin ranges from km -2. Sub basin having index 32 Difya River has the high stream frequency and the sub basin of alluvial has the low stream frequency (1.5 km -2 ). The basins of the structural hills have higher stream frequency, drainage density while the basins of alluvial has minimum. These higher values indicate that the area is occupied by Siwaliks in the lower Himalayan part and the western part by the Bomdila Group of rock. Like the drainage density, stream frequency is a similar measure of stream network of a drainage basin. Table 5.9 shows close correlation between drainage frequencies with drainage density indicating the increase in stream population with respect to increase in drainage density. To evaluate the relationship between drainage density and stream frequency, a log-log plot of drainage density vs. stream frequency is prepared. The regression line indicates the existence of direct relationship between the two parameters (Figure 5.17). Figure 5.17 Relation between Drainage density and stream frequency showing the increase of drainage frequency with drainage density 140

27 Drainage Texture (Rt) Horton (1945) defined drainage texture is the total number of stream segments of all order in a basin per perimeter of the basin. It is important to 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. 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). The drainage texture of entire 41 sub basins are of coarse to very fine. Alluvial basins show very coarse to coarse drainage texture and other basins of Himalayan part shows moderate to very fine texture. Basin north of MBT and western part of Kameng (37, 35, 32, 30, 27, and 23) shows very fine texture (8-11) with higher infiltration number ( ) reflects high drainage development. More is the texture more will be dissection and leads more erosion. Sub basins in the eastern part of Jia Bharali shows moderate to fine texture (except basin having index 11 with drainage texture 10) and the western part fine to very fine texture. 141

28 Table 5.8: Basin Index Computed Drainage density, frequency and texture of entire sub basins Basin Name Drainage Density Km -1 Drainage Frequency Km -2 Drainage Texture Km -1 1 Dipota Nadi Jorasar Nadi Mansari Nadi Dibru Nadi Khari Dikrai Nadi Upar Dikrai Nadi Daigurang Nadi Khaina Nadi Lengtey Nadi Diju Nadi Pakke River Tributary of Pakke River Tributary of Kameng River Pasa Nadi Pani Nadi Papu River Chakrasong Nadi Tributary of Pacha River Pacha River Lengpla Nadi Phuchao Nadi Kade Nala Pakoti Nadi Hoda Nadi Huduri Nadi Kaun or Hukubu Nala Gayang River Ki Nala Miao Nadi Upstream of Dinang Bru Dibri Bru Difya River Khenda Nadi Taamchin RI (Sashi Chu) Meni Nadi Nimsinggoto River Dublo Kho Tribtary of Tenga River Dogong Kho Sessa Nadi Tipi Nala

29 Basin shape The shape of the basin mainly governs the rate at which the water is supplied to the main channel. The main indices used to analyse basin shape and relief are the elongation and relief ratios. The elongation ratio is calculated by dividing the diameter of a circle of the same area as the drainage basin by the maximum length of the basin, measured from its outlet to its boundary. Three parameters viz. Elongation Ratio (Re), Circulatory Ratio (Rc) and Form Factor (Rf) are used for characterizing drainage basin shape, which is an important parameter from hydrological point of view. Elongation Ratio (Re) Schumm s 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. 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 as, Elongation ratio Shape of basin <0.7 Elongated Less elongated Oval >0.9 Circular The elongation ratio values of the different basins are varies between 0.4 and 1 (Table 5.9). The sub basins of the alluvial region shows low values ( ) represent the elongated basin with low relief. More number of sub basins in the north of MBT shows oval and circular shape. The circular basin is more efficient in run-off discharge than an elongated basin (Singh and Singh, 1997). The central parts of the Jia Bharali catchment the basins are comparatively circular with higher value than the alluvial and the piedmont zone basin. In the study area among the 41 sub basins 30 sub basins shows elongation value represents high relief and steep ground slopes. 143

30 To understand the relationship between bifurcation ratio and the elongation ratio a regression line is constructed, which show a linear negative relation i.e. with increase of elongation ratio, bifurcation ratio decrease (Figure 5.18) Figure 5.18: Graphical plot of elongation ratio and bifurcation ratio shows elongated basin have have a high bifurcation ratio. Development of lower order drainage is more in elongated basins. Circularity Ratio (Rc) The circularity ratio is a similar measure as elongation ratio, originally defined by Miller (1953), as the ratio of the area of the basin to the area of the circle having same circumference as the basin perimeter. The value of circularity ratio varies from 0 (in line) to 1 (in a circle). The Circulatory ratio for all basins is in the range of 0.23 to The Pakke River shows the lowest value, whereas the Pakoti Nadi shows the high value of Higher the value represents more circularity in the shape of the basin and vice-versa. Naturally all basins have a tendency to become elongated to get the mature stage. The observed combination of high Elongation Ratio and Circularity values, especially in the central part of the basin shows circular in nature. Some of the basins 6, 9, 16 show complicated value, high circularity ratio as well as the low elongation ratio. This complicated shape parameter is the result of the presence of a combination of lithological formations, leading to differential erosion and consequently to watershed displacement. The circularity ratio shows somewhat lower values for the basins 11 in eastern part of the study area where there is strong structural control on the drainage development. Therefore the structural control of drainage is probably responsible for the low values of circularity ratio. 144

31 Form Factor (Rf) Form factor is the numerical index (Horton, 1932) commonly used to represent different basin shapes. The value of form factor is in between Smaller the value of form factor, more elongated will be the basin. The basins with high form factors 0.8, have high peak flows of shorter duration, whereas, elongated drainage basin with low form factors have lower peak flow of longer duration. The alluvial basins shows low form factor value represent elongated in nature of the basins. The basin 13 shows high values of form factor 0.8 is ideal circular basin. The values indicate the drainage central and western part of the study area shows high values of form factor. The drainage development in these parts is high and the area has a structural control. Relation between different shape parameters Mutual relationship of these parameters can be evaluated from the plot as shown in Figure. It is found that for a given drainage basin that the elongation ratio, circularity ration and form factor show a relationship of decrease in values the order viz., elongation ratio circularity ratio > form factor. The three measures thus are conformable and suitable for defining basin shape. In four basins viz., 11, 13, 27, 35 the form factor value is complicated from the other value. This represents the structural control on the basins. The Pakke River (basin index 11) has an elongated course with curvature basins shape, totally controlled by the major trust, transverse fault and lithology of the area. Whereas the basins having index 13, 27 and 35 are of oval shape. Figure 5.19 Relation between different shape parameters shows a decrease values i.e. elongation ratio circularity ratio > form factor 145

32 Basin Index Table 5.9 Basin Name Shape parameters of entire 41 fifth order sub-basin Circularity Elongation Form Ratio (Rc) Ratio (Re) Factor (Rf) Rc=4πAu/p2 Re=2{ (Au/π)}/Lb Rf=Au/Lb 2 1 Dipota Nadi Jorasar Nadi Mansari Nadi Dibru Nadi Khari Dikrai Nadi Upar Dikrai Nadi Daigurang Nadi Khaina Nadi Lengtey Nadi Diju Nadi Pakke River Tributary of Pakke River Tributary of Kameng River Pasa Nadi Pani Nadi Papu River Chakrasong Nadi Tributary of Pacha River Pacha River Lengpla Nadi Phuchao Nadi Kade Nala Pakoti Nadi Hoda Nadi Huduri Nadi Kaun or Hukubu Nala Gayang River Ki Nala Miao Nadi Upstream of Dinang Bru Dibri Bru Difya River Khenda Nadi Taamchin RI (Sashi Chu) Meni Nadi Nimsinggoto River Dublo Kho Tribtary of Tenga River Dogong Kho Sessa Nadi Tipi Nala

33 Infiltration Number (If) The infiltration Number is defined as the product of Drainage Density (Dd) and drainage Frequency (Fs). The Jorasar Nadi has the low infiltration 2.5 and the Difya River has the higher infiltration number of ~ The Jorasar basin is found in the alluvial plain thus it has a higher infiltration. On the other hand the Dify River, in north of MBT having a higher infiltration number. The higher the infiltration number the lower will be the infiltration and consequently, higher will be run off. This leads to the development of higher drainage density. It gives an idea about the infiltration characteristics of the basin reveals impermeable lithology and higher relief. Length of Overland Flow (Lg) The term length of overland is used to describe the length of flow of water over the ground before it becomes concentrated in definite stream channels. Horton (1945) expressed it as equal to half of the reciprocal of Drainage Density (Dd). It is an important independent variable, which greatly affect the quantity of water required to exceed a certain threshold of erosion. This factor relates inversely to the average slope of the channel and is quite synonymous with the length of sheet flow to a large degree. The length of overland flow bears an effective relationship with the drainage density and constant channel maintenance. The length of overland flow ranges between Sub basin of alluvial plain (zone-i) shows high value. Sub basins of zone-ii show moderate value of 0.2 whereas the basins of zone-iii show the value of The basins north of MBT show moderate to low value. More the value represents long time of flow in the basin. The alluvial plain basins are elongated and have a high length of course. The basins of the central part have a low value, these basins have a drainage density and runoff is more but they have short course of flow. Smaller the value of overland flow the quicker surface runoff will enter the streams represents well developed drainage network with higher slope. In a relatively homogeneous area, therefore less rainfall is required to contribute a significant volume of surface runoff to stream discharge when the value of overland flow is small than when it is large. As the western part of Jia Bharali basin exhibit less rainfall than the other area, it has a quick discharge that leads to the development of the high drainage density. 147

34 Constant of Channel Maintenance (C) This parameter indicates the requirement of units of watershed surface to bear one unit of channel length. Schumn (1956) has used the inverse of the drainage density having the dimension of length as a property termed constant of channel maintenance. The drainage basins having higher values of this parameter, there will be lower value of drainage density. All the values are computed and shown in the Table (Table No 5.10). The alluvial and the piedmont area basins show comparatively high constant channel maintenance. Diputa Nadi shows highest value of 0.6 km -2 which has the least drainage density, while Difya River and the Meni Nadi has lowest constant channel maintenance of 0.3 km -2, and these two basins has the highest drainage density of 3.8 km -1 and 3.9 km -1. Higher value of constant channel Maintenance reveals strong control of lithology with a surface of high permeability. Alluvial basin of plain and piedmont zone shows highest value, as the permeability in this zone is high. 148

35 Table 5.10 Computed values of infiltration number, length of overland flow and constant of channel maintenance Basin Index Basin Name Infiltration Number Length of Over land Flow Constant of Channel Maintance If=Dd.Df Lg=1/2.Au/ Lu C=1/Dd 1 Dipota Nadi Jorasar Nadi Mansari Nadi Dibru Nadi Khari Dikrai Nadi Upar Dikrai Nadi Daigurang Nadi Khaina Nadi Lengtey Nadi Diju Nadi Pakke River Tributary of Pakke River Tributary of Kameng River Pasa Nadi Pani Nadi Papu River Chakrasong Nadi Tributary of Pacha River Pacha River Lengpla Nadi Phuchao Nadi Kade Nala Pakoti Nadi Hoda Nadi Huduri Nadi Kaun or Hukubu Nala Gayang River Ki Nala Miao Nadi Upstream of Dinang Bru Dibri Bru Difya River Khenda Nadi Taamchin RI (Sashi Chu) Meni Nadi Nimsinggoto River Dublo Kho Tribtary of Tenga River Dogong Kho Sessa Nadi Tipi Nala

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