Hydromorphogeological Study of Karawan Watershed Using GIS and Remote Sensing Techniques

2012 - Esri International User Conference

Hydromorphogeological Study of Karawan Watershed using GIS and Remote Sensing Techniques

*** Dr Kuldeep Pareta Senior Project Manager (RS/GIS & NRM) Spatial Decisions, B-30 Kailash Colony, New Delhi 110 048, India Corresponding author: [email protected]

Keywords: Geomorphology, morphometric analysis, hydrogeology, remote sensing & GIS Abstract: Resourcesat-1 LISS-IV Mx satellite imagery was used for detailed geomorphological and hydrogeological study of Karawan watershed. For morphometric analysis, ASTER data was used for preparing digital elevation model and GIS was used in evaluation of linear, areal and relief aspects of morphometric parameters. Watershed boundary, flow accumulation, flow direction, stream ordering; and contour, slope-aspect, hillshade have been prepared using ArcHydroTool; SurfaceTool in ArcGIS-10 software. Different thematic maps i.e. geological, geomorphological, lineament density, groundwater favourable zone, and drainage density have been prepared by using ArcGIS software. Authors have computed more than 85 morphometric parameter of all aspects. Based on all morphometric parameters analysis; that the erosional development of the area by the streams has progressed well beyond maturity and that lithology has had an influence in the drainage development. Author was undertaken to evaluate the groundwater prospective zones because the groundwater resources in the area have not been fully demoralized. Different hydromorphogeological units have been differentiated based on image interpretation. The hydromorphogeological units such as structural landforms, structural hills (vindhyan sediments), denudational hills (volcanic), deccan plateau, and fluvial landforms were identified and appropriate field confirmations were made. The geomorphic units such as lineaments, faults, factures, and pediplains were identified under structural landforms. The deeply and moderately weathered buried pediplains are the potential zones for groundwater targeting. Introduction: The hydromorphogeology is a recently developing branch, which have intentional of hydrology, geomorphology, and geology. The hydrology deals with surface and ground water flow; geomorphology is the science of landform, whereas geology is the study of the earth, the materials of which it is made, the structure of those materials, and the processes acting upon them. Hydromorphogeology has been defined as an interdisciplinary science that focuses on the interaction and linkage of hydrologic processes with landforms or earth materials and the interaction of geomorphic processes with surface and subsurface water in temporal and spatial dimensions (Sidle and Onda, 2004). Application of remote sensing in geology and geomorphology for quick hydro-geological evaluation has been proved very effective tool. In the present investigation lithology, hydromorphogeology, lineaments are dealt with as principal parameters for delineating groundwater favourable zones with the help of satellite imagery interpretation in combinations with conventional field methods. Detailed field checks have been carried out to confirm the observations. Further, integration of field data with general spatial data has improved the output for quantitative analysis and assessment. Study Area: This area selected for the study has not been studied in detail both from hydrogeology and from geomorphology. The watershed area of Karawan River is 289.41 Sq Kms (Fig. 1) & located between 23.74 to 23.97 N latitude and 78.59 to 78.77 E longitudes. The Karawan River originates from the southwest part of the Sagar town located at about 621 meter near the Gond village (23.74 N latitude & 78.66 E longitudes). Karawan River is 32.52 Kms long, however there is no main tributaries of the Karawan river, there are some small tributaries pouring into the river, notable amongst there are Rajauwa Nala, Garhpahara Nala on the right bank and no any major tributaries on the left bank. The Karawan River flows towards to northeast and meets the river Dhasan near Mehar village in Sagar district; Dhasan River is an important right bank tributary of the Betwa River. The study area falls in Survey of India (1:50,000) toposheets No. 55I/9, and 55I/13. The normal annual rainfall of the study area is 1234.8 mm about 90% of the annual rainfall takes place during the southwest monsoon period i.e. June to September, only 5.5% of annual rainfall takes place during winter and

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about 4.5% of rainfall occurs during the summer months. January is the coldest months with the temperature falling as low as 11.60C and max up to 24.50C, and in the month of May, the temperature goes up to 40.70C. Data Used and Methodology: Topographical Map: Survey of India (1:50,000) 55I/09, & 55I/13; ASTER (DEM) with 30m spatial resolution Remote Sensing Data: IRS-P6 (ResourceSAT-1) LISS-IV Mx satellite imagery with 5.8m spatial resolution Geological Map: Sagar District Geological Map has been collected from GSI and updated through IRS-P6 LISS-IV Mx satellite remote sensing data with limited field check Geomorphological Map: Landforms & geomorphological map have been prepared by using satellite remote sensing techniques with limited field check Morphometric Analysis: Quantitative analysis has been done based on SOI toposheets/ASTER (DEM) & different morphometric parameters have been generated in GIS environment Hydromorphogeological & Lineament Map: These maps have been prepared by using satellite remote sensing techniques with limited field check Landuse/Landcover Map: Digitally land use and land cover map has been prepared by using knowledge classification method in ERDAS IMAGINE 2010 and IRS-P6 (ResourceSAT-1) LISS-IV Mx satellite imagery and it was verified through limited field check Hydrogeological Map: The well- inventory data has been collected from primary field survey & depth to water level maps have been prepared & interpreted Results and Discussion: Geology: In order to understand the hydromorphogeological of the study area, a general lithological map has been prepared with the help of IRS-P6 (ResourceSAT-1) LISS-IV Mx satellite imagery and shown in Fig. 2. Through the general geology of the area has been mapped by the GSI in the usually way, various their similar have contributed to diverse geological aspects of the study area. Notable among these are Alexander (1979), Babu (1967), Blanford (1869), Barrooah (1962), Choubey (1967), Dixit (1970), Dubey (1952), Durge (1970), Gandhe (1970), Krishan (1982), Medlicott (1859, 1860), Mishra (1970), Pascoe (1975), Rajrajan (1978), Subramanyan (1972, 81), Wadia (1981), West (1964-81), Pareta (2004) etc. They recorded the principal rock formations namely upper vindhyan supergroup, deccan traps and intertrappean beds, and alluvium and laterite.

Figure 1: Location Map of the Study Area Figure 2: Geological Map Near by the Sagar town, comprises of hills of horizontal Vindhyan and Deccan Trap, the former commonly standing up above the level of the latter. The topography of the Vindhyan in the Sagar area is one that is characteristic of horizontal sedimentary rocks, where the highest bed is massive sandstone; the hills are generally flat topped. Southeast of the watershed, two Vindhyan hills have occurred, and between that, Berkheri village is situated. Here, for some distance around the hills, the Deccan trap has been completely removed, and the original Vindhyan topography can be seen to consist of the steep scarp slopes surrounding the two hills, with a platform between and around the hills. This platform is not neutrally horizontal, sloping gently away flow the sharps, & unlike the horizontal Deccan trap platforms, be appropriately termed a pediment. A further difference between the topography of the two formations in the study area has seen in the shapes of the contours on the scarp slopes. In the case of the Vindhyan scarps, the contours are fairly smooth, with few indentations but on the

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Deccan Trap scarps the contours are indented by many little streams which unite lower down to provide a dendrite pattern of drainage. Geomorphology: The use of remote sensing technology for geomorphological studies has definitely increased its importance due to the establishment of its direct relationship with allied disciplines, such as, geology, soils, vegetation/landuse & hydrology (Rao, 2002). The remote sensing technology is ideal for hydrological and hydro-geological studies since terrain does control movement and accumulation of surface and groundwater (Shrivastava, 1974). The author has prepared a geomorphological map (Fig. 3) by using IRS-P6 LISS-IV Mx satellite imagery, SOI maps of 1:50,000 scale, ASTER (DEM) and field observations. Geological map (structural and lithological) has also referred. The various geomorphic units and their component were identified and mapped. 1. Alluvial Plain: A level or gently sloping tract or a slightly undulating land surface produced by deposition of alluvium 2. Valley Fills: The unconsolidated sediment deposited to fill a valley. Sometime controlled by fracture forming linear depression 3. Denudational Hills (Volcanic): High relief, steep sided hills, composed mainly of basalt 4. Deccan Plateau: Low relief undulating topography, and normally cultivated soil thickness varies from place to place 5. Buried Pediment (Sandstone): Broad, gently sloping, erosional surface covered with detritus of sandstone and thin veneer of soil 6. Denudational Hill (Vindhyan Sediments): High relief, moderate to steep slope. Barren, moderate to high hills 7. Structural Hills (Vindhyan Sediments): Linear to actuate hills showing definite trend lines 8. Pediplains (Vindhyan Sediments): Thin soil covered erosional surface developed over meta-sedimentary rock i.e. quartzite, BHQ, etc. Low relief, gently sloping, undulating terrain

Figure 3: Geomorphological Map Figure 4: Stream Ordering / Drainage Map Morphometric Analysis: The measurement and mathematical analysis of the configuration of the earth's surface and of the shape and dimensions of its landform provides the basis of the investigation of maps for a geomorphological survey (Bates & Jackson, 1980). This approach has recently been termed as Morphometry. The area, altitude, volume, slope, profile and texture of landforms comprise principal parameters of investigation. Dury (1952), Christian, Jenning and Tuidale (1957) applied various methods for landform analysis, which could be classified in different ways and their results presented in the form of graphs, maps or statistical indices. The morphometric analysis of the Karawan watershed was carried out on the Survey of India topographical maps No. 55I/09, and 55I/13 on the scale 1:50,000 and ASTER-DEM with 30 m spatial resolution. The lengths of the streams, areas of the watershed were measured by using ArcGIS-10 software, and stream ordering (Fig. 4) has been generated using Strahler (1953) system, and ArcHydro tool in ArcGIS-10 software. The linear aspects were studied using the methods of Horton (1945), Strahler (1953), Chorley (1957), the areal aspects using those of Schumm (1956), Strahler (1956, 1968), Miller (1953), and Horton (1932), and the relief aspects (Fig. 5 & 6) employing the techniques of Horton (1945), Broscoe (1959), Melton (1957), Schumm (1954), Strahler (1952), and Pareta (2004). The average slope analysis of the watershed area was done using the Wentworth (1930) method. Dr Kuldeep Pareta Page 3 of 11 2012 - Esri International User Conference

The Drainage density and frequency distribution analysis of the watershed area were done using the spatial analyst tool in ArcGIS-10 software.

Figure 5: Elevation Map Figure 6: Slope Map Table 1: Drainage Network Characteristics of Karawan Watershed Su Nu Rb Nu-r Rb*Nu-r Rbwm Lu Lu/Su Lur Lur-r Lur*Lur-r Luwm Am Ar Arwm I 938 455.63 0.49 0.13 II 244 3.84 1,182 4,543.92 186.01 0.76 1.57 641.64 1,007.00 0.52 4.08 III 62 3.94 306 1204.26 99.20 1.60 2.10 285.21 598.58 2.13 4.12 3.91 IV 13 4.77 75 357.69 32.20 2.48 1.55 131.39 203.40 1.78 9.51 4.47 4.24 V 3 4.33 16 69.33 21.04 7.01 2.83 53.23 150.72 57.97 6.10 VI 1 3.00 4 12.00 15.65 15.65 2.23 36.69 81.88 219.16 3.78 Total 1261 19.88 1583 6187.20 809.72 27.99 10.28 1148.1 2,041.58 289.41 Mean 3.981 2.062 4.513 Su: Stream order, Nu: Number of streams, Rb: Bifurcation ratios, Rbm: Mean bifurcation ratio1, Nu-r: Number of stream used in the ratio, Rbwm: Weighted mean bifurcation ratios, Lu: Stream length, Lur: Stream length ratio, Lurm: Mean stream length ratio2, Lur-r: Stream length used in the ratio, Luwm: Weighted mean stream length ratio, Am: Stream order wise mean area, Ar: Area ratio, Arm: Mean area ratio3, and Arwm: Weighted mean area ratio Table 2: Hypsometric Data, and stages of Hypsometric Integrals S. No. Altitude Range (m) Height (m) h Area (Kms2) a h / H1 a / A2 % of Hi Stages 1 621 221 0.20 1.000 0.001 30 Old 2 600-621 200 7.84 0.905 0.027 30-60 Mature 3 550-621 150 44.24 0.679 0.153 60-80 Youth 4 500-621 100 93.78 0.452 0.324 80-100 Middle 5 450-621 50 221.17 0.226 0.764 100 Initial 6 400-621 0 289.41 0.000 1.000 11 = 221 m, and A2 = 289.41 Sq Kms

Hypsometric Integral = 36 % Erosional Integral = 64 %

Figure 7: Drainage Density Map Figure 8: Hypsometric Curve Dr Kuldeep Pareta Page 4 of 11 2012 - Esri International User Conference

Comparison of Drainage Basin Characteristics The details of the morphometric analysis and comparison of drainage basin characteristics of Karawan watershed are present in below table. Table 3: Comparison of Drainage Basin Characteristics of Karawan Watershed S. No. Morphometric Parameter Formula Reference Result A Drainage Network 1 Stream Order (Su) Hierarchical Rank Strahler (1952) 1 to 6 2 1st Order Stream (Suf) Suf = N1 Strahler (1952) 938.00 3 Stream Number (Nu) Nu = N1+N2+ ……Nn Horton (1945) 1261.00 4 Stream Length (Lu) Kms Lu = L1+L2 …… Ln Strahler (1964) 809.72 5 Stream Length Ratio (Lur) see table-1 Strahler (1964) 1.5-10.2 6 Mean Stream Length Ratio (Lurm) see table-1 Horton (1945) 2.06 7 Weighted Mean Stream Length Ratio (Luwm) see table-1 Horton (1945) 1.78 8 Bifurcation Ratio (Rb) see table-1 Strahler (1964) 3.0-4.7 9 Mean Bifurcation Ratio (Rbm) see table-1 Strahler (1964) 3.98 10 Weighted Mean Bifurcation Ratio (Rbwm) see table-1 Strahler (1953) 3.91 11 Main Channel Length (Cl) Kms GIS Software Analysis - 32.52 12 Valley Length (Vl) Kms GIS Software Analysis - 26.07 13 Minimum Aerial Distance (Adm) Kms GIS Software Analysis - 25.24 14 Channel Index (Ci) Ci = Cl / Adm (H & TS) Miller (1968) 1.28 15 Valley Index (Vi) Vi = Vl / Adm (TS) Miller (1968) 1.03 16 Rho Coefficient (ρ) ρ = Lur / Rb Horton (1945) 0.52 B Basin Geometry 17 Length from W’s Center to Mouth of W’s (Lcm) Kms GIS Software Analysis Black (1972) 12.93 18 Width of W’s at the Center of Mass (Wcm) Kms GIS Software Analysis Black (1972) 9.03 19 Basin Length (Lb) Kms GIS Software Analysis Schumm(1956) 26.07 20 Mean Basin Width (Wb) Wb = A / Lb Horton (1932) 11.10 21 Basin Area (A) Sq Kms GIS Software Analysis Schumm(1956) 289.41 22 Mean Area Ratio (Arm) see table-1 4.51 23 Weighted Mean Area Ratio (Arwm) see table-1 4.24 24 Basin Perimeter (P) Kms GIS Software Analysis Schumm(1956) 90.68 25 Relative Perimeter (Pr) Pr = A / P Schumm(1956) 3.19 26 Length Area Relation (Lar) Lar = 1.4 * A0.6 Hack (1957) 41.97 27 Lemniscate’s (k) k = Lb2 / A Chorley (1957) 2.34 28 Form Factor Ratio (Rf) Ff = A / Lb2 Horton (1932) 0.42 29 Shape Factor Ratio (Rs) Sf = Lb2 / A Horton (1956) 2.34 30 Elongation Ratio (Re) Re = 2 / Lb * (A / π) 0.5 Schumm(1956) 0.73 31 Elipticity Index (Ie) Ie = π * Vl2 / 4 A 1.85 32 Texture Ratio (Rt) Rt = N1 / P Schumm(1965) 9.11 33 Circularity Ratio (Rc) Rc = 12.57 * (A / P2) Miller (1953) 0.44 34 Circularity Ration (Rcn) Rcn = A / P Strahler (1964) 3.19 35 Drainage Texture (Dt) Dt = Nu / P Horton (1945) 12.06 36 Compactness Coefficient (Cc) Cc = 0.2841 * P / A 0.5 Gravelius (1914) 1.51 37 Fitness Ratio (Rf) Rf = Cl / P Melton (1957) 0.35 38 Wandering Ratio (Rw) Rw = Cl / Lb Smart & Surkan (1967) 1.24 39 Watershed Eccentricity (τ) τ = [(|Lcm2-Wcm2|)]0.5/Wcm Black (1972) 0.81 78.68 E & 40 Centre of Gravity of the Watershed (Gc) GIS Software Analysis Rao (1998) 23.86 N 41 Hydraulic Sinuosity Index (Hsi) % Hsi = ((Ci - Vi)/(Ci - 1))*100 Mueller (1968) 88.59 42 Topographic Sinuosity Index (Tsi) % Tsi = ((Vi - 1)/(Ci - 1))*100 Mueller (1968) 11.41 43 Standard Sinuosity Index (Ssi) Ssi = Ci / Vi Mueller (1968) 1.24 44 Longest Dimension Parallel to the Principal Drainage GIS Software Analysis - 30.14 Line (Clp) Kms C Drainage Texture Analysis 45 Stream Frequency (Fs) Fs = Nu / A Horton (1932) 4.35 46 Drainage Density (Dd) Km / Kms2 Dd = Lu / A Horton (1932) 2.79 47 Constant of Channel Maintenance (Kms2 / Km) C = 1 / Dd Schumm(1956) 0.35 48 Drainage Intensity (Di) Di = Fs / Dd Faniran (1968) 1.55 49 Infiltration Number (If) If = Fs * Dd Faniran (1968) 12.13 50 Drainage Pattern (Dp) Horton (1932) Dn&Ra 51 Length of Overland Flow (Lg) Kms Lg = A / 2 * Lu Horton (1945) 0.17 D Relief Characterizes

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52 Height of Basin Mouth (z) m GIS Analysis / DEM - 447.00 53 Maximum Height of the Basin (Z) m GIS Analysis / DEM - 621.00 54 Total Basin Relief (H) m H = Z - z Strahler (1952) 174.00 55 Relief Ratio (Rhl) Rhl = H / Lb Schumm(1956) 0.006 56 Absolute Relief (Ra) m GIS Software Analysis 621.00 57 Relative Relief Ratio (Rhp) Rhp = H * 100 / P Melton (1957) 0.19 58 Dissection Index (Dis) Dis = H / Ra Singh & Dubey (1994) 0.28 59 Channel Gradient (Cg) m / Kms Cg = H / {(π/2) * Clp} Broscoe (1959) 1.83 60 Gradient Ratio (Rg) Rg = (Z - z) / Lb Sreedevi (2004) 0.006 61 Watershed Slope (Sw) Sw = H / Lb 0.0067 62 Ruggedness Number (Rn) Rn = Dd * (H / 1000) Patton & Baker (1976) 0.48 63 Melton Ruggedness Number (MRn) MRn = H / A0.5 Melton (1965) 10.22 64 Total Contour Length (Ctl) Kms GIS Software Analysis - 1591.54 65 Contour Interval (Cin) m GIS Software Analysis - 10.00 66 Length of Two Successive Contours (L1+L2) Km GIS Software Analysis Strahler (1952) 194.38 67 Average Slope Width of Contour (Swc) Swc = A / {(L1+L2) / 2} Strahler (1952) 2.98 68 Slope Analysis (Sa) GIS Analysis / DEM Rich (1916) 200’-702’ 69 Average Slope (S) % S = (Z * (Ctl/H)) / (10 * A) Wenthworth’s (1930) 1.96 70 Mean Slope Ratio (Sm) Wenthworth’s (1930) 2.03 71 Weighted Mean Slope Ratio (Swm) Wenthworth’s (1930) 2.64 72 Mean Slope of Overall Basin (Ѳs) Ѳs = (Ctl * Cin) / A Chorley (1979) 0.54 73 Relative Height (h/H) see table-2 (h/H ) Strahler (1952) 100 to 0 74 Relative Area (a/A) see table-2 (a/A ) Strahler (1952) 0 to 100 75 Hypsometric Integrals (Hi) % Hypsom Curve h/H & a/A Strahler (1952) 36.00 76 Erosional Integrals (Ei) % Hypsom Curve h/H & a/A Strahler (1952) 64.00 77 Clinographic Analysis (Cga) Tan Q = Cin / Awc Strahler (1952) 2.98 78 Erosion Surface (Es) m Superimposed Profiles Miller (1953) 490-500 79 Surface Area of Relief (Rsa) Sq Kms Composite Profile Brown (1952) 289.41 80 Composite Profile Area (Acp) Sq Kms Area between the Composite Curve and Pareta (2004) 289.41 Horizontal Line 81 Minimum Elevated Profile Area as Projected Profile Area between the Minimum Elevated Pareta (2004) 236.43 Profile as Projected Profile and (App) Sq Kms Horizontal Line 82 Erosion Affected Area (Aea) Sq Kms Aea = Acp - App Pareta (2004) 52.98 Area between the Curve of the Profile and 83 Longitudinal Profile Curve Area (A1) Sq Kms Snow & Slingerland (1987) 85.34 Horizontal Line Triangular Area created by that Straight 84 Profile Triangular Area (A2) Sq Kms Snow & Slingerland (1987) 157.88 Line, the Horizontal Axis Traversing the Head of the Profile

85 Concavity Index (Ca) Ca = A1 / A2 Snow & Slingerland (1987) 0.54 Hydromorphogeology: A combined analysis of landforms (geomorphology), rocks as well as structures (geology) such as faults, folds, fractures etc. in relation to groundwater occurrence aspects with the help of remote sensing of ground truth is considered very useful in preparing integrated Hydro-geomorphogeologic Maps for targeting groundwater (Pareta, 2011). Ray and Raina (1973) attempted to describe the hydro- geomorphological units coupled with geological parameters in Kotipally catchment area of Hyderabad. Chatterji et al. (1978) studied Central Luni basin of western Rajasthan using remote sensing data. Raju and Vaidyanadhan (1984) used remote sensing techniques in the study of Sarada river basin. Similar studies on other river basins of India were also attempted such researchers as Raviprakash and Mishra, 1993; Mangrulkar, et al., 1993, Thomas, et al., 1995; Saini and Nathawat, 1996. Hydro-geomorphological map of the study area was prepared using IRS-P6 LISS-IV Mx data; and following hydro-geomorphological units are delineated on the hydro-geomorphological map (Fig. 9). ƒ Alluvial Plain (AP) ƒ Valley Fills (VF) ƒ Denudational Hill (Volcanic) (DNH-V) ƒ Deccan Plateau (DP) ƒ Buried Pediment (Sandstone) (BP-SST) ƒ Denudational Hill (Vindhyan sediments) (DNH-VC) ƒ Structural Hills (Vindhyan Sediments) (SH-VC) ƒ Pediplains (Vindhyan Sediments) (PP-VC) ƒ Dykes (DYK) ƒ Lineaments (LNMT)

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To find the fracture density of these hydro-geomorphic units, lineaments have been marked on the hydro- geomorphological map. It indicates that the alluvial plain (AP), valley fills (VF), Buried pediments (BP-SST), and lineaments (LNMT) are excellent hydro-geomorphic units from the view of occurrence and movement of groundwater. They are good groundwater potential zones of the study area. The description of different hydro- geomorphic units of Karawan watershed has been given in Table-4 and depicted in Fig. 9. Table 4: Hydromorphogeological Units of Karawan Watershed Map Geomorphic Lithology Structure Description or Ground Water Symbol Units Characteristics Occurrence AP Alluvial Constitutes gravel, - A level or gently sloping Good to excellent Plain sand, silt, or clay tract or a slightly depending upon sized unconsolidated undulating land surface alluvium thickness material produced by deposition of alluvium VF Valley Fills Constitutes boulders, The Valleys The unconsolidated Good to excellent cobbles, pebbles, sometimes sediment deposited to fill depending upon gravels, sand, silt, and fracture a valley. Sometime type of lithology and clay sized grains of controlled controlled by fracture thickness of the varying lithology forming linear depression material deposited DNH (V) Denudationa Composed of basalt Jointed and High relief, steep sided Poor, except along l Hill of deccan traps fractured hills, composed mainly of lineament and (Volcanic) basalt. depressions DP Deccan Composed of basalt Jointed and Low relief undulating Moderate, good Plateau of deccan traps fractured topography. Normally along lineaments cultivated soil thickness weathered zone and varies from place to place depressions BP(SST) Buried Vindhyan sand stone - Broad, gently sloping, Moderate Pediment dominating the erosional surface covered (Sand Stone) underlying lithology with detritus of sandstone and thin veneer of soil DNH (VC) Denudationa Composed of sand Jointed and High relief, moderate to Poor, moderate l Hill stone, siltstone etc. of fractured steep slope, barren, along liniments (Vindhyan Vindhyan super moderate to high hills weathered zones, sediments) group and depressions SH(VC) Structural Composed of sand Associated Linear to actuate hills Poor, moderate to Hills stone, silt stone etc. of with folding, showing definite trend good along linear (Vindhyan Vindhyan super faulting etc. lines inner hill valleys Sediments) group DYK Dykes Intrusive of quartz - Quartz intrusions that cut Moderate to good on across the rock up gradient LNMT Lineaments Cut across various Fault, Fault line, fractures, Good, excellent at lithology fractures etc. joints, shear zone, contact inter section of zones, other linear lineament features and straight stream courses Lineament Structure: Lineaments play significant role in groundwater exploration particularly in hard rocks. Water well yields often show a positive correlation with linear features or with the intersection of two features (Gold, 1980; Moores et al, 1992). Therefore, groundwater prospecting based on mapping of landforms and lineaments (Hydro- morphogeological mapping) is now very common using remote sensing data (Sahai et al., 1991; Sahai et al. 1993; Shrivastava and Bhattacharya, 2000). Lineaments are defined as linear features of geological significance extending in length over several kilometres. These linear features usually represent faults, fractures or shear zones and are identified on satellite images on the basis of tonal contrast, stream/river alignment, and differences in vegetation and knick-points in topography. Lineament study of the area from remotely sensed imagery provides important information on sub-surface fractures that may control the movement and storage of groundwater (Pareta, 2004). Therefore, a lineament map of the study area has been prepared using IRS-P6 LISS-IV Mx data. A glance at this map shows that there are four predominant sets of lineaments present in the basalt. One set of lineament trend NE-SW whereas the other striking NW-SE. The fracture density is more in the Rajauwa, Kanera, Ratona, Semrahat, Kanchri, and Deori Village (Fig. 10).

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Figure 9: Hydromorphogeological Map Figure 10: Lineament Density Map Land Use and Land Cover: Land is the most important natural resource, which embodies soil, water and associated flora and fauna involving the total ecosystem (Rao et al., 1996). Comprehensive information on the spatial distribution of land use/land cover categories and the pattern of their change is a prerequisite for management and utilization of the land resources of the study area. The land use pattern of any terrain is a reflection of the complex physical processes acting upon the surface of the earth. These processes include impact of climate, geologic and topographic conditions on the distribution of soils, vegetation and occurrence of water. For better development and management of the catchment areas, it is necessary to have timely and reliable information on environmental status. Keeping the above views in mind, the authors have prepared a land use/land cover map (Fig. 11) using IRS-P6 LISS-IV Mx data (Fig. 12). This figure depicts that there are four units of land cover/land use pattern in the study area, which are given below and shown on the map. Agricultural land: Fallow Land, Land with Shrub; Open Land; Forest: Deciduous Forest, Degraded Forest; Water Features

Figure 11: Land Use / Land Cover Map Figure 12: IRS-P6 LISS-IV MX Satellite Imagery Hydrogeology: The well inventory data of 13 dug wells have been collected through primary field survey for pre-monsoon and post -monsoon, 2010 (Table 5). These data relate to different rock formations occurring in the region, viz., alluvium, basalt, and sandstone. Pre-monsoon and post-monsoon depths to water level maps have been generated by using point interpolation method in ArcGIS-10 software, and well inventory data (Fig. 13 & 14). A glance at pre-monsoon depth to water level map indicates that the depth ranges between 4.83 m bgl and more than 12.14 m bgl in Karawan watershed. It is evident that depth to water level is mostly deep to moderate in the Dr Kuldeep Pareta Page 8 of 11 2012 - Esri International User Conference

major part of the watershed except a small area in the north-west part where it is very deep (Fig. 13). About 80% area of the watershed shows the deep to moderate water level, and about 15% shows the very deep water level, which indicates heavy pumping of ground water through dug wells and tube wells. A glance at post-monsoon depth to water level map indicates that depth to water level ranges between 2.32 m to 6.29 m bgl in the watershed. The major part of the area shows shallow moderate depth to water level except in the pockets around Kanera, Rajauwa, Ratona, Berkheri Khurd, Northeast of Sagar Town, Pagara, Nearby Garhpahara, Semra Hat, and Deori (Fig. 14). Table 5: Hydrogeological Data of Inventoried Wells S. No. Location Lithology T. D. R. L. D. W. Pre (DTWL) Post (DETWL) FLU 1 Sarkhadi Basalt 11.50 523.61 4.40 10.47 5.99 4.48 2 Berkheri Basalt 5.35 496.12 3.8 4.83 2.32 2.51 3 Sihora Basal 12.95 503.12 3.53 12.14 6.29 5.85 4 Semadhana Basalt 6.90 518.35 2.82 7.70 3.75 2.95 5 Rajauwa Basalt 10.00 502.45 5.10 7.47 3.07 4.40 6 Sagar Basalt 13.80 548.70 6.05 9.18 6.16 3.02 7 Baroda Basalt 7.25 522.58 4.35 7.18 4.36 2.82 8 Naryawali Sandstone 9.50 495.60 2.85 8.49 4.63 3.86 9 Jaruakheda Basalt 10.95 497.81 2.99 9.87 6.18 3.69 10 Mehar Basalt 9.30 504.28 3.97 7.42 4.97 2.45 11 Ranipura Sandstone 9.40 478.39 3.80 6.63 3.30 3.33 12 Paharguwa Sandstone 10.30 491.79 5.05 8.40 4.77 3.63 13 Bandri Sandstone 12.40 519.25 4.85 9.68 4.09 5.59 T. D.: Total Depth (m) below ground level (bgl), R. L.: Reduced Level of Ground Level (m), Diameter of Well (m), Pre (DTWL): Pre- Monsoon Depth to Water Level (m) bgl, Post (DTWL): Post-Monsoon Depth to Water Level (m) bgl, FLU: Fluctuation

Figure 13: Pre-Monsoon DTWL Map Figure 14: Post-Monsoon DTWL Map Surface investigations of groundwater are seldom more than partially successful in that results usually leave the hydro-geologic picture incomplete; however, such methods are normally less costly than subsurface investigations (Singhal et al., 1988). Remote sensing from satellite has become an increasingly valuable tool for understanding subsurface water conditions. The occurrence and movement of groundwater depend upon the rock formations present in the area. It also depends upon the topography, structure, and geomorphology, as well as hydro-geological properties of the water-bearing materials. The hydrogeological properties of water-bearing formation with a view to throw light on any possibility of inflow of ground waters from the hard rock as well as unconsolidated hydro-litho units into the aquifers of the study area. Alluvium comprises of silt, sand, gravel, and clay particles, it is an excellent aquifer; basalt belongs to deccan traps, and sandstone belongs to vindhyan supergroup, it is a moderate aquifer in the study area. Depth to water level represents the position of water table with reference to ground surface. A groundwater favourable zonation of the study area has been analysed by the using of ModelBuilder Application in ESRI ArcGIS-10 with the lithological structural, geomorphology & landform, drainage density, hydro-geomorphological elements, lineament density, land use, and the background of the survey of India topographical maps on 1:50,000 scale. On the basis of integration of these maps groundwater favourable zones of the study area were identified. The groundwater favourable zones are shown in Fig. 15. On the above

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considerations, the various hydromorphogeological units have then been classified into five categories of groundwater potentiality namely, very good, good, moderate, poor and very poor. The hydromorphogeological unit such as alluvial plain, valley fills, deccan plateau, buried pediment (sand stone) are most favourable zones for groundwater exploration & development in the study. Hence, these areas are marked as good to very good favourable zones. These zones are distributed mostly in the northwest, middle, and southwest portion of the study. A glance at Fig. 15 reveals that the northern part and some of the southern part of the study area have excellent groundwater potential as compared to the south-eastern part of the watershed. This information is very useful for the further groundwater development in the study area.

Figure 15: Groundwater Favourable Zone Map of Karawan Watershed Conclusion: Hydromorphogeology analysis is a simple tool with not much of initial expenditure to study the river basin within the four walls of the laboratory and choose the areas of the possible groundwater potentials for further concentrated field studies. This analysis reduces the field expenditure; the large amounts of time consumed and enhance the quality of results. Remote sensing techniques with an emphasis on geology, geomorphology, physiography, hydro- geomorphology, structure, geo-hydrology, land use/land cover help in identification of the potential zones for developmental planning and predicting limitations to their implementation with reasonable accuracy. Lineaments particularly joints/fractures and their intersection appear to be potential sites for groundwater exploitation. The valley fills and burried pediments are good groundwater potential zones. Acknowledgement: The author is grateful to Mr Kapil Chaudhery, Director Spatial Decisions New Delhi for providing the necessary facilities to carry out this work. I am also thankful to my Guru Ji Prof. J. L. Jain for the motivation of this work.

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References: [1] Broscoe, A.J. (1959), Quantitative Analysis of Longitudinal Stream Profiles of Small Watersheds, Project N. 389-042, Tech. Bep. 18, Columbian Uni Dept. Geol., ONR, Geography Branch, New York. [2] Calef, W. C. (1950), Form and Process, Cambridge University Press, London, pp. 473. [3] Chorley, R.J. (1972), Spatial Analysis in Geomorphology, Mathuen and Co. Ltd., London. [4] Chorley, R.L. (1967), Models in Geomorphology, in R.J. Chorley and P. Haggett (eds.), Models in Geography, London, pp. 59-96. [5] Dury, G.H. (1952), Methods of Cartographical Analysis in Geomorphological Research, Silver Jubilee Volume, Indian Geographical SOCIETY, Madras, pp. 136-139. [6] Faniran, A. (1968), The Index of Drainage Intensity - A Provisional New Drainage Factor, Aus. Jour. of Sci., vol. 31, pp. 328-330. [7] Gold, D. P. (1980), Structural Geology, Chapter 14 in Remote Sensing in Geology, edit by Siegal, B. S. and Gillespie, A. R., John Wiley, New York, pp. 410-483. [8] Gregory, K.J. & Walling, D.E. (1968), The Variation of Drainage Density within a Catchment, Inst. Assoc. Sci. Hydrol., Bulletin, 13, pp. 61-68. [9] Horton, R.E. (1932), Drainage Basin Characteristics, Trans. Am. Geog. Union. Vol-13, pp-350-61. [10] Horton, R.E. (1945), Erosional Development of Streams and their Drainage Basins, Bull. Geol. Soc. Am. Vol.-56, pp- 275-370. [11] King, C.A.M. (1966), Techniques in Geomorphology, Edward Arnold, (Publishers) Ltd. London, pp. 319-321. [12] Melton, M.A. (1957), An Analysis of the relations among Elements of Climate, Surface Properties and Geomorphology, Project NR 389042, Tech. Rep. 11, Columbia University. [13] Pareta, K. (2003), Morphometric Analysis of Dhasan River Basin, India, Uttar Bharat Bhoogol Patrika, Gorakhpur, Vol. 39, pp. 15-35. [14] Pareta, K. (2004), Hydro-Geomorphology of Sagar District (M.P.): A Study through Remote Sensing Technique, Proceeding in XIX M. P. Young Scientist Congress, Madhya Pradesh Council of Science & Technology (MAPCOST), Bhopal. “Winning Best Paper Award” [15] Pareta, K. (2005), Rainfall-Runoff Modelling, Soil Erosion Modelling, Water Balance Calculation, and Morphometric Analysis of Molali Watershed, Sagar, Madhya Pradesh using GIS and Remote Sensing Techniques, Proceeding in 25th International Cartographic Congress, INCA. [16] Pareta, K. (2010), Advance Remote Sensing and GIS Technologies for Hydrological Study and Groundwater Exploration in Bhansar & Budhil Watershed, Himachal Pradesh, Proceeding in Applications of Geoinformatics for National Development (AGNDAM), Dr. Hari Singh Gour University, Sagar. [17] Pareta, K. (2011”a”), Geo-Environmental and Geo-Hydrological Study of Rajghat Dam, Sagar (Madhya Pradesh) using Remote Sensing Techniques, International Journal of Scientific & Engineering Research Volume 2, Issue 8 (ISSN 2229- 5518), pp. 1-8. [18] Pareta, K. (2011”b”), Impacts of Land Use and Climate Change Scenarios on the Water Flux: A Case Study of Sal River Watershed, Chamba (H. P.), Proceeding in 12th ESRI India User Conference, Noida (INDIA), pp. 1-9. [19] Pareta, K. and Koshta, Upasana (2009), Soil Erosion Modeling using Remote Sensing and GIS: A Case Study of Mohand Watershed, Haridwar, Madhya Bharti Journal, Dr. Hari Singh Gour University, Sagar (M.P.), Vol. No. 55, pp. 23-33. [20] Richards, K. S. Arnett, R. R. and Ellis, J. (1985), Geomorphology and Soils, George Allen and Unwin, London, pp. 441. [21] Scheidegger, A.E. (1965), The Algebra of Stream Order Number, U.S. Geol. Survey Prof. Paper 525B, B1, pp. 87-89. [22] Schumm, S.A. (1954), The relation of Drainage Basin Relief to Sediment Loss, Internet. Assoc. Sci. Hyd. Pub. 36, pp. 216-219. [23] Schumm, S.A. (1956), Evolution of Drainage Systems & Slopes in Badlands at Perth Anboy, New Jersey, Bull. Geol. Soc. Amer. 67, pp. 597-646. [24] Schumm, S.A. (1963), Sinuosity of Alluvial Rivers on the Great Plains, Geol. Soc. Amer. Bull. 74, pp. 1089-1100. [25] Shreve, R.L. (1966), Statistical Law of Stream Numbers, J. Geol. 74, pp. 17-37. [26] Smith, G. H. (1939), The Morphometry of Ohio: The Average Slope of the Land (abst.), Annals Assoc. Am. Geogr. Vol. 29, pp. 94. [27] Strahler, A.N. (1952 “a”), Dynamic Basis of Geomorphology, Bull. Geol. Soc. Am., Vol. 63, pp. 923-938. [28] Strahler, A.N. (1952 “b”), Hypsometric Analysis of Erosional Topography, Bull. Geol. Soc. Am. Vol-63. pp. 1117-42. [29] Strahler, A.N. (1956), Quantitative Slope Analysis, Bull. Geol. Soc. Am., Vol. 67, pp. 571-596. [30] Strahler, A.N. (1964), Quantitative Geomorphology of Drainage Basin and Channel Network, Handbook of Applied Hydrology, pp-39-76. [31] Thornbury, W.D (1954), Principles of Geomorphology, John Wiley and Sons, London. [32] Wentworth, C. K. (1930), A Simplified Method of Determining the Average Slope of Land Surfaces, Am. J. Sci., Vol. 21, pp. 184-194. [33] Woldenberg, N.J. (1967), Geography & Properties of Surface, Handward Paper in Theoretical Geography, Vol.1 pp. 95- 189.

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