ations along the 
alous SL values 
: downward part 
| uniformly. The 
L 2500; 300« 
hat are observed 
ctonic activities, 
reams flow over 
when they are 
duced by strike- 
  
  
?5'5320"E 
lues. 
tect the presence 
scale. The Af is 
Pinter, 2002). 
(2) 
e right (facing 
total area of the 
may result from 
> tectonics or 
stream slipping 
etry factor was 
well developed 
ulated Af values 
etween 0.17 and 
W regions of the 
s those near the 
s were classified 
Af «7. 
t describes the 
landscape. The 
lage basin and is 
rresponds to the 
s correlated with 
). We have used 
al., 2010) of the 
n resolution for 
of hypsometric 
range from 0.14 
especially those 
  
situated in the middle and lower parts of the basin show low Hi 
values. But sub-basins with structural contro] show convex 
hypsometric curves and high integral values. The values were 
classified into three categories: Hi 20.5; Hi«0.5 Hi 7 0.4; and 
<0.4. 
u 
À 
     
    
12" 18 407M 
32 8'0"N 
115320"N 
10.282036 
f ES 
ees e Ld 
  
  
  
  
75°48 WE TS°I00PE TS"AY'AD E 795320E 
Figure 3. Spatial distribution of Af values. 
  
x 
1275'0"N 42^168'40"N 
11:53720"N 
vo PSII AH 
  
  
  
754820°E 75°300°E T5'AVAUE T553'207E 
Figure 4. Spatial distribution of Hi values. 
4.4 Index of drainage basin shape (Bs) 
Drainage basin shape is an elongation ratio and describes the 
planimetric shape of a basin. It is expressed as: 
Bs= Bl/Bw (3) 
where, Bl is length of the basin measured from its mouth to the 
most distal point in the drainage divide, and Bw is width of the 
basin measured across the short axis between left and right 
valleys divides (Ramirez-Herrera, 1998). The index reflects 
differences between elongated basins with high values of Bs 
associated with relatively higher tectonic activity, and more 
circular basins with low values generally associated with low 
tectonic activity. Relatively young drainage basins in active 
tectonic areas tend to be elongated in shape normal to the 
topographic slope of a mountain. In the study area, majority of 
the sub-basins show moderate to high Bs values which indicate 
elongated nature of the sub-basins (Figure 5). The values were 
classified into three categories: Bs >3; Bs <3 Bs>2; and <0.2. 
  
T289"N T2*16/407N. 
115320 
118-263 
184-218 
  
& 3 *6 
OY. ARR + 5:2 404 
  
  
   
River 
BBW 75300" TE 4TACE 75'S320"E 
Figure 5. Spatial distribution of Bs values. 
4.5 Ratio of valley floor width to valley height (Vf) 
The Vf ratio is a good measure that indicates whether the river is 
actively down cutting and incising (Bull and McFadden, 1977). 
Vf was calculated by using equation (4). 
Vf-Vfw/[(Eld-Esc)*(Erd-Esc)y2] (4) 
where, Vf is the ratio of valley floor width to valley height; Vfw 
is the width of the valley floor; Eld is the elevation of the divide 
on the left side of the valley; Erd is the elevation on the right 
side; and Esc is the average elevation of the valley floor. This 
index has been applied to evaluate the relative degree of tectonic 
activity of several mountain fronts located in the eastern and 
central Betic Cordillera (Silva et al, 2003). The index is a 
measure of incision and not uplift; but in an equilibrium state, 
incision and uplift are nearly matched. For each of the selected 
basin, the requisite valley width and height data were obtained 
along valley cross-sections perpendicular to the drainage basin 
axis and calculated the Vf (Figure 6). The values were classified 
into three categories: Vf«0.39; Vf 20.55 Vf«1.05; and Vf 71.2. 
i 
  
x 
À 
1271640"N 
TPSOUW 
  
  
  
  
g 
8 
2 
>= 
BH 554-008 2 % © 2 
GN River IORI WERNE Hi REA 
75°18'20°F 7530 0"E TSATAOE 75°5320°E 
Figure 6. Spatial distribution of Vf values. 
4.6 Relative tectonic activity classes 
All the five geomorphic indices show anomalous high values in 
the river capture areas and low values above the Ghat region. The 
relative tectonic activity classes (Iat) were obtained by compiling 
all the five geomorphic indices. Based on the value of each