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- Taylor & Francis
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- © 2019 The Author(s). Published by Informa UK Limited, trading as Taylor & Francis Group on behalf of the International Water, Air & Soil Conservation Society(INWASCON).
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- 2474-9508
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Abstract
GEOLOGY, ECOLOGY, AND LANDSCAPES 2020, VOL. 4, NO. 4, 288–297 INWASCON https://doi.org/10.1080/24749508.2019.1694130 RESEARCH ARTICLE Morphometric analysis of landforms on basalt, granite gneiss and schist geological formations in north Karnataka, India – a comparison P.L. Patil, G.S. Dasog , S.A. Yerimani, V. B. Kuligod, M. Hebbara and S.T. Hundekar Department of Soil Science & Agricultural Chemistry, University of Agricultural Sciences, Dharwad, India ABSTRACT ARTICLE HISTORY Received 5 June 2019 Morphometric analysis reveals the development of land surface processes and provides an Accepted 7 September 2019 insight into hydrologic behaviour of watershed. A morphometric analysis of landforms on basalt, granite gneiss and schist in north Karnataka was conducted with the objective of KEYWORDS comparing various morphometric parameters among them. A sub-watershed each was Comparative morphometry; selected to represent landform on basalt, granite gneiss and schist. The stream length was DEM; drainage pattern; highest in sub-watershed on basalt and was least on schist with one on granite gneiss being geological formations; sub- intermediate. The stream number was highest in basalt and its values were similar in granite watersheds gneiss and schist. Total relief, relief ratio and ruggedness number were distinctly high in sub- watershed on schist compared to the other two. The low mean bifurcation ratios in all three sub-watersheds suggested stability of the landforms. Drainage density was relatively coarser in the sub-watershed on granite-gneiss compared to the other two. The drainage network was dendritic in the sub-watershed on basalt, sub-dendritic on granite gneiss and sub-trelis on schist. The drainage texture and texture ratio were slightly higher, overland flow values were lower in sub-watersheds on basalt and schist compared to that on granite-gneiss. All three sub- watersheds exhibited similar elongation ratio, form factor and circularity ratio. Introduction geologic diversity with formations ranging from the Archean granites, granite gneisses, and schists through Morphometry is the measurement and mathematical Holocene basalts to Pre-Cambrian sedimentary rocks analysis of the configuration of the earth’s surface, to recent alluvium. Granite gneiss occupies dominant shape and dimension of its landforms (Agarwal, area in the state of Karnataka with considerable area of 1998; Obi Reddy, Maji, & Gajbhiye, 2002). basalts, especially in the northern and north western Hydrologic and geomorphic processes occur within part and schist scattered all around (Radhakrishna & a watershed. Therefore, morphometric characteriza- Vaidynadhan 2011). Karnataka state is a pioneer in tion at the watershed level brings out the information watershed development works in India. Presently, it is on development of land surface processes and pro- implementing Sujala-3 Watershed Development pro- vides an insight into the hydrologic behaviour of ject with World Bank funding in 11 districts of the a watershed (Altaf, Meraj, & Ramshoo, 2013; Singh, state including Vijayapur, Koppal and Gadag. Basalt is 1992). Morphometric analysis also helps to under- the predominant geological formation in Vijayapur stand initial slope or inequalities in the rock hardness, district and granite gneiss is the dominant geology in structural controls, recent diastrophism, geological both Koppal and Gadag districts, with considerable and geomorphic history of drainage basin (Strahler, area under chlorite schist in both the districts. 1964). These studies are made for a range of objectives Therefore, it was of interest to see the land surface including prioritization of watersheds (Biswas, processes on these three important geological forma- Sudhakar, & Desai, 1999), to understand ground tions under similar overhead climate. Vittala, water hydrology (Nag & Chakraborty 2003), to study Govindaiah, and Honnegowda (2004) studied mor- the drainage network as influenced by bedrock geol- phometry of a watershed in granite gneiss terrain in ogy (Nag & Chakraborty 2003; Sameena, southern Karnataka and Yasmin, Sateeshkumar, Krishnamurthy, & Jayaraman, 2009) and others. Ayyangoudar, and Narayanrao (2013) in Raichur dis- Extensive use of GIS techniques for assessing various trict in northern Karnataka. There are many other terrain and morphometric parameters of the drainage studies on morphometry on granitic landscapes of basins and watersheds has been the hallmark of these south India (Sreedevi, Owais, Khan, & Ahmed, 2009; studies, as they provide a flexible environment and Wilson, Chandrasekar, & Magesh, 2012). Similarly, a powerful tool for the manipulation and analysis of Sahu et al. (2010) made a morphometric analysis of spatial information. Karnataka is known for its basaltic terrain in sub-humid central India. Altaf et al. CONTACT G.S. Dasog gdasog@gmail.com Department of Soil Science & Agricultural Chemistry, University of Agricultural Sciences, Dharwad, India © 2019 The Author(s). Published by Informa UK Limited, trading as Taylor & Francis Group on behalf of the International Water, Air & Soil Conservation Society(INWASCON). This is an Open Access article distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited. GEOLOGY, ECOLOGY, AND LANDSCAPES 289 (2013) studied the morphometry of Lidder river valley Climate in Kashmir on sedimentary formations. However, All the three sub-watersheds are located in the semi- a comparative study of morphometry under a similar arid area of north Karnataka described as Northern Dry climate on different geological formations are few zone (zone-3) agro-climatically. Dindur sub-watershed (Krishnamurthy, Srinivas, Jayaram, & is somewhat more humid than the other two. The Chandrasekhar, 1996; Nag & Chakraborty 2003) and climatic and other ancillary data is furnished in Table 1. none for northern Karnataka. Therefore, this study was made to compare the morphometric properties Geology, geomorphology and slope among the three landforms on the three major geolo- The Dadamatti sub-watershed is occupied by the gical formations under a similar overhead semi-arid basaltic flows of Deccan traps, which belong to the climatic condition in north Karnataka. sequence of Middle Deccan Traps of Upper Cretaceous to Lower Eocene Age. The basalts are generally dark grey to black in colour, fine grained, Study area highly vesicular and zeolitic in nature. The sub- Location watershed has predominantly pediments, pediplains For this study, three sub-watersheds occurring on three and floodplain along the river Doni. different geological formations were selected. These The granite gneiss landscape is moderately plain with three sub-watersheds include Dadamatti on basalt in shallow troughs and mounds of granites hills at scat- Vijyapura district, Belageri on granite-gneiss in Koppal tered places in rugged topography with highest peaks. district and Dindur sub-watershed on chlorite-schist in The hard granite-gneissic rocks do not have any pri- Gadag district. The location of these sub-watersheds, mary porosity; however, weathering, fracturing, joints their constituent micro-watersheds and the drainage and tectonic features like folds and faults have secondary network is shown in Figure 1. Dadamatti sub- porosity and permeability (Central Ground Water watershed comprises of seven micro-watersheds, Board (CGWB), 2008). Weathered thickness is reported Belageri of 11 and Dindur sub-watershed of eight to vary from a minimum of one metre to a maximum of micro-watersheds. The area of the former two is similar 20 m nearer to streams. In general, ground water is whereas that of Dindur is less than both. available in the weathered zone under phreatic Figure 1. Location map of sub-watersheds studied. 290 P. L. PATIL ET AL. Table 1. Salient features of the sub-watersheds selected. Temperature ºC Rain fall Sub-watershed Geology mm Max Min Slope No. of wells Predominant soils Dadamatti Basalt 565.0 33.6 19.6 Nearly all the area has 1–3% 165 70% area calcareous Vertisols and 20% Lithic Ustorthents, Belageri Granite gneiss 559.6 36.5 20.4 1/3rd area 0–1% and 922 Lithic and Typic Haplustalfs, remaining 1–3% Ustepts and Vertisols Dindur Schist 628.0 32.1 19.2 Area distributed equally 160 Lithic Ustorthents and Lithic among 1–3%, 3–5% and Haplustepts >5% condition and under confined to semi-confined condi- were measured, computed and outputs generated tions in the jointed and fractured formation. usingArc GIS10.4. Theformulaeemployedforcom- The Gadag schist belt consists of a 2000 m thick pile putation of various morphometric parameters are pre- of meta-volcanics and meta-sediments. The structural sented in Table 2.The DEMofthe threesub-watersheds deposition of the belt is the result of an overall E–W was generated by using SRTM data of 90 m resolution compressional regime with uplift and diaperism of the to highlight the relief features (Figure 2). sialic basement. These rocks have no primary porosity or permeability; ground water occurs under a phreatic Results and discussion condition in weathered zone of these formations. Nearly, all of the sub-watershed area on both basalt Linear aspects and granite gneiss is nearly level to very gently sloping Linear aspects such as stream order, stream number lands except for 1% area with slopes 3–5%. In sharp for various orders, bifurcation ratio, stream lengths for contrast to these two, the sub-watershed on schist has various stream orders and stream length ratio are considerable area (35%) under gently sloping lands with described below. slope class of 3–5%, followed by 19% area under mod- erately sloping lands with slope range of 5–10% and strongly sloping area (8%) with a slope of 10–15% range. Stream number The sub-watersheds on basalt and granite-gneiss had Soils and erosion fifth order streams and the one on schist had fourth Very deep black soils (Vertisols) predominate in order stream (Table 3), This is perhaps due to the Dadamatti sub-watershed with appreciable portion of smaller area of the sub-watershed on schist compared shallow and very shallow black soils occupying higher to the other two as basin area is known to increase elements of topography. The soils of Beligeri sub- exponentially with stream order as per law of areas watershed comprise of moderately deep (75–100 cm) (Schumm, 1956). The number of streams decreased as and deep (100–150 cm) red soils (Haplustalfs) and the stream order increased in all the three sub- associated black soils (Haplusterts). Dindur sub- watersheds. In all of them, first order stream numbers watershed comprises mainly very shallow (<25 cm) constitute nearly 50% and second order 25% of the and shallow (25–50 cm) and to some extent moderately total as observed elsewhere (Magesh, Jiteshlal, shallow fine textured red soils in 75% area and black Chandrashekar, & Jini, 2013). At first, second and soils (Vertisols and vertic Inceptisols) in the remaining third order, the number of streams in sub-watershed area. on basalt was roughly one and a half times more than Both Dadamati and Belegeri sub-watersheds are that observed in other two sub-watersheds. There was predominantly moderately to slightly eroded. The similarity between sub-watersheds on granite gneiss Dindur stands out with 42% area affected by severely and schist with respect to number of streams at differ- and very severely eroded class compared to 4% area in ent orders. The total number of streams was highest in Beligeri and under 1% in Dadamatti. the sub-watershed on basalt followed by a similar number in those on granite gneiss and schist. Similar trend was observed in the component micro- Methodology watersheds as well. The sub-watershed maps were prepared by geo- Whereas the first and second order streams were referencing and merger of high resolution Liss IV and observed in all the sub-watersheds, the third order CARTOSAT data at a scale of 1:7920. The drainage streams were present in all the micro-watersheds of network layer has been converted to digital format Dadamatti, five in Beligeri and four in Dindur. The through on-screen digitization using Arc GIS ver. 10.4 fourth order streams were present in three micro- software from the image employing Survey of India watersheds of Dadamatti, in two of Belageri but none toposheets (1:50,000) as reference. Various entities of Dindur. GEOLOGY, ECOLOGY, AND LANDSCAPES 291 Table 2. Computation methods used to derive various morphometric parameters described in the study. Sl. No Morphometric Parameter Formula Reference 1 Stream order Hierarchical rank Strahler (1964) 2 Stream length (Lu) Length of the stream Horton (1945) 3 Mean stream length (Lsm) Lsm = Lu/Nu; where Lu = total stream length of order “u” Strahler (1964) and Nu = Total no. of stream segments of order “u” 4 Stream length ratio (RL) RL = Lu/Lu-1 where, Lu = total stream length of order (u), Horton (1945) and Lu-1 = the total stream length of its next lower order 5 Bifurcation ratio (Rb) Rb = Nu/Nu+1; where, Nu = Total number of stream Schumm (1956) segment of given order, Nu+1 = Total number of segments of next of given order 6 Mean bifurcation ratio (Rbm) Rbm = Average of bifurcation ratios of all orders Strahler (1957) 7 Total relief (H) Total relief is difference between maximum and minimum elevation in the sub-watershed 8 Relief ratio (Rr) Rh = H/Lb; Where, H = total relief and Lb = basin length Schumm (1956) 9 Ruggedness number (Rn) Rn = H*D where H = total relief (Km) and D = drainage Strahler (1964) density (Km/Km ) 9 Elongation ratio (Re) Re = {2×Sqrt(A/π)}/Lb where, A = Area of the basin and Schumm (1956) Lb = Basin length 8 Drainage density (D) D = Lu/A; where Lu = total stream length of all orders (Km) Horton (1932) and A = area of the basin (Km ) 9 Drainage texture (Dt) Rt = Nu/P; where, Nu = total number of streams of all Horton (1945) orders and P = perimeter of basin (Km) 10 Texture ratio (Rt) T = N1/P; where, N1 = total number of first order streams Horton (1932) and P = perimeter of basin (Km) 13 Stream frequency (Fs) Fs = Nu/A; where, Nu = total number of streams of all Horton (1932) orders and A = basin area 14 Form factor (Rf) Rf = A/(Lb) ; where, A = Area of basin and Horton (1932) Lb = basin length 2 2 15 Circularity ratio (Rc) Rc = (4π × A)/P , where A = area of basin (Km ) and Miller (1953) P = perimeter of basin (Km) 16 Length of overland flow Lg = 1/2×D; where D = drainage density Horton (1945) Stream length watershed on schist followed similar trend as in basalt The difference among the three sub-watersheds is but in absolute terms it was lowest compared to the more clearly brought out in length of the stream. other two ranging from 0.42 to 3.08. Wilson et al. The total length of all streams and that of first order (2012) also observed an increase in mean stream stream is highest in the sub-watershed on basalt fol- length with increase in order in sub-watersheds on lowed by that on granite gneiss and was least in the granitic terrain in Tamil Nadu with some exceptions sub-watershed on schist. The length of second, fourth as observed in this study. and fifth order streams were similar in sub-watershed A plot of log stream number against stream order on basalt and granite gneiss, and were lesser than both (Figure 3(a)) conforms to the law of stream numbers in that on schist. The length of third order streams in (Horton, 1945) which states that the number of streams sub-watersheds on granite gneiss and schist were simi- of different orders in a given drainage basin tends to lar but distinctly less than in basalt. approximate an inverse geometric ratio in respect of all Mean stream length reflects the size of component the three sub-watersheds. Similarly a plot of log mean drainage network and its contributing surface and is stream length against stream order (Figure 3(b)) con- directly proportional to the size and topography of the forms to law of stream length (Horton, 1932)which drainage basin. It is observed that the mean stream states that the average length of streams of each of the length values for any stream order are greater than differentordersina drainage basintends closelyto that of the lower order. The mean stream length approximate a direct geometric ratio. This suggests increased from 0.83 in first order to 4.24 km in fourth that the basin evolution followed the erosion laws act- order in the sub-watershed on basalt (Table 3). ing on geologic material with homogenous weathering- Whereas the difference between the first and erosion characteristics (Sameena et al., 2009)with no the second order was not much, it was more than upliftment of the basins (Altaf et al., 2013). twice between second and third and between third and fourth. In the sub-watershed on granite gneiss Stream length ratio terrain, however, the mean stream length in first Stream length ratio varied in a rather narrow range order was comparable to that of basalt but unlike in among the sub-watersheds but varied widely in respect basalt the difference was twice as much between first of component micro-watersheds of all the three sub- and second and increased by a smaller magnitude in watersheds. For example, the stream length ratio varied subsequent orders with maximum in fourth order like from 0.34 to 0.57 in the sub-watershed on basalt, from in basalt. The mean stream length in the sub- 0.36 to 0.86 in that on granite-gneiss and from 0.52 to 292 P. L. PATIL ET AL. Figure 2. Digital elevation models of the three sub-watersheds. 0.70 in the sub-watershed on schist. However, the range II in all the three sub-watersheds. According to Horton presented by the constituent micro-watersheds varied (1945) bifurcation ratio of 2–3 indicate flat region. In the considerably from 0.02 to 1.75 for the sub-watershed on present study the mean Br values are in a narrow range of basalt, from 0.18 to 2.28 in that on granite-gneiss and 3.07–3.23, which fall under normal basin category accord- from 0.14 to 3.48 in the sub-watershed on schist; a trend ing to Strahler (1957). He demonstrated that the bifurca- of increasing upper limit was observed going from tion ratio shows a small range of variation for different basalt to schist. The stream length ratio increased stea- regions or different environmental conditions, except dily from lower order to higher order in the sub- where the geology dominates.The variationinrespect of watersheds on both basalt and schist suggesting their both Br and mean Br was more among the component mature geomorphic stage of development (Vittala et al., micro-watersheds in all the three sub-watersheds with 2004). An inconsistent trend was observed in the sub- highest in granite gneiss sub-watershed. The mean bifur- watershed on granite gneiss. cation ratios of the sub-watersheds and their component micro-watersheds are within the range 3.0–5.0 suggesting that the influence of geological structures on the drainage Bifurcation ratio network is negligible. Therefore, all the sub-watersheds Bifurcation ratio may be defined as the number of stream have suffered least structural disturbances. segments of given order to the number of segments of the next higher order (Schumm, 1956). It is considered as an index of relief and dissection (Horton, 1945). Bifurcation Drainage pattern ratio varied from 2.0 to 4.5 in sub-watershed on basalt, 2.0–4.75 in granite gneiss and in a narrow range of 3.00– The drainage pattern is dendritic in sub-watersheds on 3.33 in schist. Further, the highest Br was observed in III/ basalt and sub-dendritic in granite gneiss but sub- GEOLOGY, ECOLOGY, AND LANDSCAPES 293 Table 3. Linear properties of the sub-watersheds and their component micro-watersheds studied. No. of streams in different orders Order wise Stream Length (Km) Micro-watershed Area (Km ) Length (Km) Perimeter (Km) Stream order I II III IV V Total I II III IV V Total BASALT (DADAMATTI SUB-WATERSHED) MWS-1 9.37 6.59 16.47 4 19 7 2 1 29 13.37 5.84 2.84 0.40 22.45 MWS-2 5.55 3.60 10.22 3 10 3 1 14 8.33 6.99 0.27 15.59 MWS-3 5.30 4.15 12.64 3 13 4 1 18 11.70 2.90 5.07 19.67 MWS-4 7.22 4.27 11.62 3 11 2 1 14 10.60 3.80 0.99 15.39 MWS-5 7.71 4.12 12.92 3 11 2 1 14 9.85 5.20 0.57 15.62 MWS-6 5.89 4.06 10.40 3 16 3 1 20 11.24 1.88 1.76 14.88 MWS-7 10.03 4.95 15.25 4 18 6 2 1 27 14.77 7.64 5.62 0.11 28.14 Sub-watershed 51.07 11.59 36.89 5 92 27 6 2 1 128 75.92 25.93 14.98 8.48 3.60 128.91 GRANITE GNEISS (BELIGERI SUB-WATERSHED) MWS-1 4.73 3.35 9.73 2 4 1 5 2.32 3.08 5.40 MWS-2 3.76 4.01 14.51 2 7 1 8 4.26 0.32 4.58 MWS-3 5.08 4.34 11.90 2 7 1 8 6.57 3.14 9.71 MWS-4 4.55 3.91 11.67 2 8 1 9 5.51 2.67 8.18 MWS-5 3.94 5.15 13.53 1 3 3 6.29 6.29 MWS-6 4.48 4.54 12.09 2 8 1 9 4.76 1.91 6.67 MWS-7 4.00 5.09 14.50 2 3 1 4 1.96 4.46 6.42 MWS-8 7.07 4.85 15.17 3 9 2 1 12 10.11 1.83 2.18 14.42 MWS-9 4.52 3.61 10.72 3 10 3 1 14 5.17 3.96 1.22 10.35 MWS-10 6.69 4.04 11.50 3 13 4 1 18 8.22 3.82 1.57 13.61 MWS-11 6.48 3.73 13.92 4 12 5 2 1 20 7.28 3.05 2.16 0.39 12.88 Sub-watershed 55.31 11.93 41.04 5 67 19 4 2 1 93 51.63 25.88 9.20 7.89 3.65 98.25 SCHIST (DINDUR SUB-WATERSHED) MWS-1 3.90 3.57 9.44 3 8 3 1 12 2.09 2.57 3.29 7.94 MWS-2 2.82 3.13 8.85 2 4 1 5 2.97 1.32 4.29 MWS-3 3.76 2.64 9.24 3 13 3 1 17 4.71 0.64 2.23 7.58 MWS-4 4.52 2.72 8.56 3 13 4 1 18 5.17 3.01 2.50 10.68 MWS-5 5.09 3.59 10.42 3 13 4 1 18 5.76 2.72 1.32 9.80 MWS-6 3.14 3.69 9.71 3 12 3 1 16 4.28 1.93 2.10 8.31 MWS-7 3.62 3.32 9.39 2 2 1 3 1.08 1.40 2.48 MWS-8 2.93 2.64 7.27 2 5 2 7 1.88 0.64 2.52 Sub-watershed 29.77 7.52 28.44 4 63 20 6 2 91 26.29 13.74 8.85 6.15 55.03 Micro-Watershed Mean Stream Length in Km (Lsm) Stream Length Ratio (RL) Bifurcation Ratio (Rb) Mean Bifurcation Ratio (Rbm) I II III IV V II/I III/II IV/III V/IV I/II II/III III/IV IV/V BASALT (DADAMATTI SUB-WATERSHED) MWS-1 0.70 0.83 1.42 0.40 0.44 0.49 0.14 0.00 2.71 3.5 2.0 2.74 MWS-2 0.83 2.33 0.27 0.84 0.04 0.00 3.33 3.0 3.17 MWS-3 0.90 0.73 5.07 0.25 1.75 0.00 3.25 4.0 3.63 MWS-4 0.96 1.90 0.99 0.36 0.26 0.00 5.50 2.0 3.75 MWS-5 0.90 2.60 0.57 0.53 0.11 0.00 5.50 2.0 3.75 MWS-6 0.70 0.63 1.76 0.17 0.94 0.00 5.33 3.0 4.17 MWS-7 0.82 1.27 2.81 0.11 0.52 0.74 0.02 0.00 3.00 3.0 2.0 2.67 Sub-watershed 0.83 0.96 2.50 4.24 3.60 0.34 0.58 0.57 0.42 3.41 4.5 3.0 2.0 3.23 GRANITE GNEISS (BELIGERI SUB-WATERSHED) MWS-1 0.58 3.08 0.00 0.00 0.00 1.33 0.00 0.00 0.00 4.00 0.00 0.00 0.00 4.00 MWS-2 0.61 0.32 0.00 0.00 0.00 0.08 0.00 0.00 0.00 7.00 0.00 0.00 0.00 7.00 MWS-3 0.94 3.14 0.00 0.00 0.00 0.48 0.00 0.00 0.00 7.00 0.00 0.00 0.00 7.00 MWS-4 0.69 2.67 0.00 0.00 0.00 0.48 0.00 0.00 0.00 8.00 0.00 0.00 0.00 8.00 MWS-5 2.10 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 MWS-6 0.60 1.91 0.00 0.00 0.00 0.40 0.00 0.00 0.00 8.00 0.00 0.00 0.00 8.00 MWS-7 0.65 4.46 0.00 0.00 0.00 2.28 0.00 0.00 0.00 3.00 0.00 0.00 0.00 3.00 MWS-8 1.12 0.92 2.18 0.00 0.00 0.18 1.19 0.00 0.00 4.50 2.00 0.00 0.00 3.25 MWS-9 0.52 1.32 1.22 0.00 0.00 0.77 0.31 0.00 0.00 3.33 3.00 0.00 0.00 3.17 MWS-10 0.63 0.96 1.57 0.00 0.00 0.46 0.41 0.00 0.00 3.25 4.00 0.00 0.00 3.63 MWS-11 0.61 0.61 1.08 0.39 0.00 0.42 0.71 0.18 0.00 2.40 2.50 2.00 0.00 2.30 Sub-watershed 0.77 1.36 2.30 3.95 3.65 0.50 0.36 0.86 0.46 3.53 4.75 2.00 2.00 3.07 SCHIST (DINDUR SUB-WATERSHED) MWS-1 0.26 0.86 3.29 0.00 1.23 1.28 0.00 2.67 3.00 2.83 MWS-2 0.74 1.32 0.00 0.00 0.44 0.00 0.00 4.00 0.00 4.00 MWS-3 0.36 0.21 2.23 0.00 0.14 3.48 0.00 4.33 3.00 3.67 MWS-4 0.40 0.75 2.50 0.00 0.58 0.83 0.00 3.25 4.00 3.63 MWS-5 0.44 0.68 1.32 0.00 0.47 0.49 0.00 3.25 4.00 3.63 MWS-6 0.36 0.64 2.10 0.00 0.45 1.09 0.00 4.00 3.00 3.50 MWS-7 0.54 1.40 0.00 0.00 1.30 0.00 0.00 2.00 0.00 2.00 MWS-8 0.38 0.32 0.00 0.00 0.34 0.00 0.00 2.50 0.00 2.50 Sub-watershed 0.42 0.69 1.48 3.08 0.52 0.64 0.70 3.15 3.33 3.0 3.16 trelis on schist, thus pointing the effect of lithology arid climatic regions of southern Karnataka (Figure 2). A dendritic to sub-dentritic drainage pat- (Krishnamurthy et al., 1996) and in much humidor tern on Peninsular gneiss and trellis to sub-trellis climate of West Bengal (Nag & Chakraborty, 2003) drainage pattern on schistose formations in semi- was documented. 294 P. L. PATIL ET AL. Figure 3. (a) Plot of number of streams vs stream order. (b) Plot of mean stream length vs stream order. Relief characteristics the low values with valleys and pediments (Sreedevi et al., 2009). The relief properties bring out the influence of aspect and height over a basin area. Total relief ratio and ruggedness number were studied. Total relief was high- Drainage texture analysis est in sub-watershed on schist followed by granite Drainage texture analysis includes drainage density, gneiss and basalt (Table 4). The constituent micro- stream frequency and length of overland flow. watersheds on schist presented a wide variation in relief Drainage density is a measure of landscape dissection compared to granite gneiss and basalt. According to and runoff potential, infiltration capacity of the land relative relief classification by Melton (1957)sub- and vegetation cover of the catchment and it is known watersheds on both basalt and granite gneiss exhibit to influence the output of water and sediment from the low relative relief (<100 m) and that on schist a medium catchment area and erosion susceptibility (Soni, 2016). relative relief (100–300 m). Both the relief ratio and Drainage density was least in the sub-watershed on ruggedness numbers were highest in sub-watershed granite-gneiss followed by basalt and schist. on schist and both these parameters were considerably Krishnamurthy et al. (1996) also recorded similar less in the case of sub-watersheds on granite gneiss and values for the watershed on Peninsular gneiss in basalt (Table 4). The relief ratio and ruggedness num- southern Karnataka. The drainage texture was coarse ber of the constituent micro-watersheds on schist in all the three sub-watersheds as the values were in exhibited wide variability compared to the micro- the range of 2–4 (Smith, 1950). However, the value watersheds of the other two sub-watersheds. The high was distinctly less in the watershed on granite gneiss values are associated with hilly areas and mounds and GEOLOGY, ECOLOGY, AND LANDSCAPES 295 Table 4. Relief and gradient parameters of the sub-watersheds and their component micro-watersheds studied. Total Relief Ruggedness Drainage Texture Drainage Stream fre- Form Circu lar- Elonga Length of relief ratio no. texture ratio density (D) quency (Fs) factor ity ratio tion ratio overland Watershed Name (m) (Rr) (Rn) (Dt) (Rt) (km/km ) (km/Km (Rf) (Rc) (Re) flow (Lg) BASALT (DADAMATTI SUB-WATERSHED) MWS-1 36 0.005 0.11 1.76 1.15 3.09 2.40 0.22 0.43 0.52 0.16 MWS-2 23 0.006 0.06 1.37 0.98 2.52 2.81 0.43 0.67 0.74 0.20 MWS-3 30 0.007 0.10 1.42 1.03 3.39 3.71 0.31 0.42 0.63 0.15 MWS-4 40 0.009 0.08 1.20 0.95 1.94 2.13 0.40 0.67 0.71 0.26 MWS-5 29 0.007 0.05 1.08 0.85 1.82 2.03 0.46 0.58 0.76 0.27 MWS-6 35 0.009 0.12 1.92 1.54 3.40 2.53 0.36 0.68 0.67 0.15 MWS-7 35 0.007 0.09 1.77 1.18 2.69 2.81 0.41 0.54 0.72 0.19 Sub-watershed 53 0.005 0.13 3.47 2.49 2.51 2.52 0.38 0.47 0.70 0.20 GRANITE GNEISS (BELIGERI SUB-WATERSHED) MWS-1 33 0.010 0.03 0.51 0.41 1.06 1.14 0.42 0.63 0.73 0.47 MWS-2 40 0.010 0.09 0.55 0.48 2.13 1.22 0.23 0.22 0.55 0.24 MWS-3 37 0.009 0.06 0.67 0.59 1.57 1.91 0.27 0.45 0.59 0.32 MWS-4 50 0.013 0.10 0.77 0.69 1.98 1.80 0.30 0.42 0.62 0.25 MWS-5 47 0.009 0.04 0.22 0.22 0.76 1.60 0.15 0.27 0.43 0.66 MWS-6 35 0.008 0.07 0.74 0.66 2.01 1.49 0.22 0.39 0.53 0.25 MWS-7 39 0.008 0.04 0.28 0.21 1.00 1.61 0.15 0.24 0.44 0.50 MWS-8 34 0.007 0.06 0.79 0.59 1.70 2.00 0.30 0.39 0.62 0.29 MWS-9 32 0.009 0.10 1.31. 0.93 3.09 2.29 0.35 0.49 0.66 0.16 MWS-10 47 0.012 0.13 1.57 1.13 2.69 2.03 0.41 0.64 0.72 0.19 MWS-11 30 0.008 0.09 1.44 0.86 3.09 1.99 0.47 0.42 0.77 0.16 Sub-watershed 89 0.007 0.15 2.27 1.63 1.68 1.78 0.39 0.41 0.70 0.30 SCHIST (DINDUR SUB-WATERSHED) MWS-1 151 0.042 0.47 1.27 0.85 3.08 2.04 0.31 0.46 0.62 0.16 MWS-2 69 0.022 0.12 0.56 0.45 1.77 0.52 0.29 0.45 0.61 0.28 MWS-3 172 0.065 0.78 1.84 1.41 4.52 2.01 0.54 0.55 0.83 0.11 MWS-4 106 0.039 0.42 2.10 1.52 3.98 2.36 0.61 0.78 0.88 0.13 MWS-5 87 0.024 0.31 1.73 1.25 3.54 1.93 0.39 0.59 0.71 0.14 MWS-6 163 0.044 0.83 1.65 1.24 5.10 2.65 0.23 0.42 0.54 0.10 MWS-7 58 0.017 0.05 0.32 0.21 0.83 0.69 0.33 0.52 0.65 0.60 MWS-8 56 0.021 0.13 0.96 0.69 2.39 0.86 0.42 0.70 0.73 0.21 Sub-watershed 218 0.043 0.67 3.20 2.21 3.06 1.85 0.53 0.55 0.82 0.16 than the other two and a majority of component former will travel faster compared to that on basalt and micro-watersheds had values of less than 1. schist (Krishnamurthy et al. 1996). A relatively lower drainage density and drainage tex- ture in the sub-watersheds on granite gneiss underpins Basin geometry the relatively higher permeability of the weathered rock and of the predominantly red soils they have in The varying slopes of watershed can be classified with this sub-watersheds. Large number of wells (Table 1) the help of the index of elongation ratio, i.e. circular in this sub-watershed holds testimony to this. Relative (0.9 ~ 0.10), oval (0.8 ~ 0.9), less elongated (0.7 ~ 0.8), spacing of channels in a drainage basin is expressed by elongated (0.5 ~ 0.7) and more elongated (less than texture ratio (Rt) and drainage texture (Dt). Relatively 0.5). The three sub-watersheds can be termed as less higher values of Rt and Dt were observed in MWS 9, elongated as they exhibited elongation ratio of 0.70–- 10 and 11 of granite gneiss and, MWS 3 and 5 of schist 0.82 and conform to the observation by Strahler situated in the upper reaches (Figure 2). High values (1957) that elongation ratio runs between 0.6 and 1.0 are generally found in the upper reaches and low over a wide variety of climatic and geologic types. values near the mouth (Biswas, Majumdar, & Elongated basins are known to have low Rb values Banerjee, 2014). and circular basins have high Rb values (Verstappen, The texture ratio and stream frequency values of sub- 1983). The form factor was remarkably similar in the watershed on basalt were distinctly different from those sub-watersheds on basalt and granite gneiss with that on granite-gneiss and schist (Table 4). Fs values of all the on schist exhibiting slightly higher value. However, the sub-watersheds have close relation with Dd indicating component micro-watersheds exhibited considerable the increase in stream population with increase in drai- variability. Smaller the value of form factor, more nage density. The stream frequency was more in basalt elongated will be the watershed and these watersheds compared to granite gneiss and schist. However, the would experience low peak flows for longer duration. component micro-watersheds on schist presented The circularity ratio is the ratio of basin area to the a wider range than those on granite gneiss. The length area of a circle having the same perimeter as the basin of overland flow was distinctly greater in the sub- (Strahler, 1964). The ratio approaching one indicates watershed on granite gneiss compared to those on basalt that the basin is circular. The circularity ratios varied and schist suggesting that the surface runoff in the from 0.41 in the sub-watershed on granite gneiss to 296 P. L. PATIL ET AL. 0.55 in that on schist with sub-watershed on basalt ORCID lying in between, suggesting all are far from being G.S. Dasog http://orcid.org/0000-0002-7009-743X circular. However, the component micro-watersheds exhibited some variability with the highest observed in the sub-watershed on granite gneiss with a circulatory References ratio ranging from 0.22 to 0.64. Agarwal, C. S. (1998). Study of drainage pattern through aerial data in Naugarh area of Varanasi district, U.P. Conclusions Journal of the Indian Society of Remote Sensing, 26, 169–175. A morphometric analysis of landforms on basalt, Altaf, F., Meraj, G., & Ramshoo, S. A. (2013). Morphometric granite gneiss and schist in north Karnataka was con- analysis to infer hydrological behaviour of Lidder ducted with the objective of comparing various mor- watershed, Western Himalayas, India. Geography Journal, 14. Article ID 178021. doi:10.1155/2013/178021. phometric parameters among them. The total number Biswas, A., Majumdar, D. D., & Banerjee, S. (2014). of streams as well as length of first order stream was Morphometry governs the dynamics of a drainage highest in the sub-watershed on basalt compared to basin: Analysis and implications. Geography Journal, 14. those on granite gneiss and schist. The stream number Article ID 927176. doi:10.1155/2014/927176. values were similar in granite gneiss and schist. The Biswas, S., Sudhakar, S., & Desai, V. R. (1999). Prioritization of sub-watersheds based on morphometric analysis of stream length was highest in sub-watershed on basalt drainage basin: A remote sensing and GIS approach. and was least on schist with one on granite gneiss Journal of the Indian Society of Remote Sensing, 27, being intermediate. The drainage network was den- 155–166. dritic in the sub-watershed on basalt, sub-dendritic on Central Ground Water Board (CGWB). (2008). Groundwater granite gneiss and sub-trelis on schist. Total relief, information booklet of Koppal district, Karnataka (pp. 19). relief ratio and ruggedness number were distinctly Bangalore: CGWB South Western Region. Horton, R. E. (1932). Drainage basin characteristics. high in sub-watershed on schist compared to the Transactions American Geophysical Union, 13, 350–361. other two. Drainage density was relatively coarser in Horton, R. E. (1945). Erosional development of streams and the sub-watershed on granite-gneiss compared to the their drainage basins: Hydrophysicalapproach to quanti- other two. The drainage texture and texture ratio were tative morphology. Geological Society of America Bulletin, slightly higher, overland flow values were lower in 56, 275–370. Krishnamurthy, J., Srinivas, G., Jayaram, V. M., & sub-watersheds on basalt and schist compared to that Chandrasekhar, G. (1996). Influence of rock type and on granite-gneiss. 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Journal
Geology Ecology and Landscapes – Taylor & Francis
Published: Oct 1, 2020
Keywords: Comparative morphometry; DEM; drainage pattern; geological formations; sub-watersheds