- Open Access
- Total Downloads : 11
- Authors : Sudha V, Gayathri M S, Arun Babu A V, Jose Paul Manickath, Kishore Dev C
- Paper ID : IJERTCONV4IS20009
- Volume & Issue : GEOSPATIAL – 2016 (Volume 4 – Issue 20)
- Published (First Online): 24-04-2018
- ISSN (Online) : 2278-0181
- Publisher Name : IJERT
- License: This work is licensed under a Creative Commons Attribution 4.0 International License
Mapping the Spatial Extend of Groundwater Level using Geostatistical Techniques: A Case Study Around the Area of Palakkad, Kerala, India
Sudha V1
Associate Professor, NSS College of engineering,
Palakkad, Kerala
Gayathri M S2, Arun Babu A V2, Jose Paul Manickatp, and Kishore Dev C2
UG Student, NSS College of engineering, Palakkad, Kerala
Abstract-Information of the ground water levels in an aquifer is a need for the sustainable management of the ground water resources. But the limited number of, monitoring sites in a given aquifer are not always sufficient to accurately represent the water table. Geostatistical methods can be used to predict the groundwater level at unvisited locations of an aquifer. This paper deals with the application of Geostatistics for the spatial analysis of groundwater level of Palakkad region.
Keywords- Ground Water, Geostatistics, Groundwater level, ordinary Kriging, semivariogram.
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NTRODUCTION
Successful management of groundwater resources using numerical models requires knowledge of spatial distribution of hydraulic heads, aquifer parameters and other input data. Spatial interpolation techniques play a vital role in sustainable management of groundwater system by estimating the model input parameters at regular grid points from their measurements at random locations.There are two main groupings of spatially interpolation techniques: deterministic and geostatistical. Deterministic interpolation techniques create surfaces from measured data based on either the extent of similarity (inverse distance weighted) or the degree of smoothing (radialbasis functions). Geostatistical interpolation techniques utilize the statistical properties of the measured data to produce the raster maps (M.I. Kamali et al.2015). Geostatistics requires considerable computational effort, including two critical and time-consuming processes: estimation of the semivariogram and determination of the best fitted semivariogram model. However, geostatistics often yields the most accurate estimates, because it takes the spatial structure of the variables into account, and, in addition, enables the quantification of corresponding estimation errors. Geostatistics is including different types of Kriging method such as Ordinary, Simple, Universal, Probability, Indicator, Disjunctive and Cokriging. Kriging quantifies the spatial correlation of the data which is called variography and then presents a prediction for the locations without any measured data.
A number of studies have been conducted to determine the depth to ground water level in theother parts of the world.
Bernard Ofosu et al (2014) successfully demonstrated how ground water level can be mapped integrating GIS with borehole data. Available depth to ground water level information can be used to determine the effects of ground water on civil engineering structures during the preliminary investigations. Borehole information on ground water level across Ashanti region for 37 observation wells was used to predict the depth to ground water level. The data was interpolated using kriging interpolation techniques in a GIS environment. Map showed ground water level is spatially distributed.A case study by Vijay Kumar (2007) describes how universal kriging can be used to interpolate hydraulic heads in an area where measurements are made at random places. The technique is appliedfor the estimation of groundwater levels for the post-monsoon period of 1990 in an arid area of Rajasthan State, India. The unbounded omni- directional semivariogram indicates the presence of drift in groundwater levels and so the need for universal kriging. Considering the semivariogram in the direction of least drift as the underlying semivariogram, the drift order was estimated by a cross-validation procedure.Mevlut Uyan etal they conducted a study to determine and evaluate the spatial changes in the depletion of groundwater level differences by using geostatistical methods based on data from 58 groundwater wells during the period from April 1999 to April 2008.The Determination of Reference Evapotranspiration for Spatial Distribution Mapping Using Geostatistics by M.I. Kamali et al. (2015) the study compares two approaches for preparation of spatial distribution maps of ET0 in Mazandaran province of Iran. The differences between the interpolation methods are more depended strongly on the nature of the variables under study, data spatial configuration, number of available samples, the assumption drawn and the selected criteria for the interpolation than the method of interpolation.
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STUDY AREA
The study area selected is Palakkad district of Kerala(Fig.1), located in the realm of tropical climate lying between 10°2111°14N lat. and 76°02 – 76°54E long. Palakkad is a major Paddy growing area of the State.The annual rainfall
varies from 1883 to 3267 mm based on long term normal
.The district receives on an average 2362 mm of rainfall annually.
Groundwater in the district is mostly developed through dug wells and bore wells for domestic, agricultural and for industrial needs. A good percentage of the households in the district have their own drinking water wells. Recently the bore well culture has picked up and gained momentum in the district.
collected from the groundwater department, Kerala. The year 2009 was selected for the study. The stasticaltable shows ground water level data
WELL NO
MAX W L
MIN W L
AVG WL
Northing
Easting
114
6.76
8.83
7.90
1189778
622676.6
115
5.12
7.82
7.02
1194226
629111.3
116
1.79
3.28
2.52
1189840
638642.2
134
2.03
7.95
6.10
1203135
644162
PKD S-11
3.54
12.88
6.46
1195860
649660.6
PKD S-12
5.31
10.10
7.82
1191329
650555.8
PKD S-5
5.99
10.81
8.74
1214225
650779.8
PKD S-10
4.70
11.60
9.37
1205278
653444.2
157
4.28
12.24
9.29
1197763
654791
122
1.43
4.16
2.85
1173895
659496.3
135
6.48
12.22
9.40
1215593
659406.6
160 PKD-1
7.75
11.39
9.98
1215483
659516.4
152
6.73
11.72
8.57
1194475
661148.6
PKD S-9
3.04
7.90
5.49
1194476
661257.9
121 PKD
1.88
4.92
3.45
1171254
662353.8
128
1.78
4.80
3.44
1192829
663671.8
PKD S-14
1.44
6.16
3.71
1215950
664541.1
130
2.59
7.20
4.88
1200141
666259.9
132
3.76
9.25
7.28
1204576
668205.5
PKD S-2
0.57
1.64
0.93
1177145
668343.2
PKD S-4
1.97
4.49
3.09
1186442
669500.1
129
4.00
9.68
7.54
1193749
670884.9
131
0.38
3.62
1.83
1198405
672719.9
160 PKD-12
1.05
2.67
1.61
1184920
674649.1
123
0.71
2.33
1.56
1171538
675046.3
PKD S-3
0.70
4.62
2.10
1185586
675083.2
160 PKD-5
0.2
4.18
2.27
1190899
675711.7
PKD S-15
3.06
7.30
5.46
1196012
680496.5
127
4.44
7.90
6.25
1191146
680632.1
PKD S-1
1.48
5.64
3.07
1181970
681556.6
149
0.4
6.12
2.58
1172017
682047.6
160 PKD-10
2.83
4.82
3.78
1192598
683139.8
148
2.3
5.48
3.6
1172598
687078.6
126
1.61
5.71
3.38
1183787
690189.4
133
0.33
5.23
3.02
1194078
690787.4
PKD S-8
2.70
6.40
3.83
1178154
691643.6
151
2.99
5.84
4.22
1186467
694550.1
PKD S-7
0.17
5.02
2.09
1187497
700451.4
WELL NO
MAX W L
MIN W L
AVG WL
Northing
Easting
114
6.76
8.83
7.90
1189778
622676.6
115
5.12
7.82
7.02
1194226
629111.3
116
1.79
3.28
2.52
1189840
638642.2
134
2.03
7.95
6.10
1203135
644162
PKD S-11
3.54
12.88
6.46
1195860
649660.6
PKD S-12
5.31
10.10
7.82
1191329
650555.8
PKD S-5
5.99
10.81
8.74
1214225
650779.8
PKD S-10
4.70
11.60
9.37
1205278
653444.2
157
4.28
12.24
9.29
1197763
654791
122
1.43
4.16
2.85
1173895
659496.3
135
6.48
12.22
9.40
1215593
659406.6
160 PKD-1
7.75
11.39
9.98
1215483
659516.4
152
6.73
11.72
8.57
1194475
661148.6
PKD S-9
3.04
7.90
5.49
1194476
661257.9
121 PKD
1.88
4.92
3.45
1171254
662353.8
128
1.78
4.80
3.44
1192829
663671.8
PKD S-14
1.44
6.16
3.71
1215950
664541.1
130
2.59
7.20
4.88
1200141
666259.9
132
3.76
9.25
7.28
1204576
668205.5
PKD S-2
0.57
1.64
0.93
1177145
668343.2
PKD S-4
1.97
4.49
3.09
1186442
669500.1
129
4.00
9.68
7.54
1193749
670884.9
131
0.38
3.62
1.83
1198405
672719.9
160 PKD-12
1.05
2.67
1.61
1184920
674649.1
123
0.71
2.33
1.56
1171538
675046.3
PKD S-3
0.70
4.62
2.10
1185586
675083.2
160 PKD-5
0.2
4.18
2.27
1190899
675711.7
PKD S-15
3.06
7.30
5.46
1196012
680496.5
127
4.44
7.90
6.25
1191146
680632.1
PKD S-1
1.48
5.64
3.07
1181970
681556.6
149
0.4
6.12
2.58
1172017
682047.6
160 PKD-10
2.83
4.82
3.78
1192598
683139.8
148
2.3
5.48
3.6
1172598
687078.6
126
1.61
5.71
3.38
1183787
690189.4
133
0.33
5.23
3.02
1194078
690787.4
PKD S-8
2.70
6.40
3.83
1178154
691643.6
151
2.99
5.84
4.22
1186467
694550.1
PKD S-7
0.17
5.02
2.09
1187497
700451.4
Table 1
3.2Geostatistical Analysis
Fig 1 The Location of study area
The ground water level fluctuation varies from 2 to 4 m bgl and the maximum fluctuation is noticed in the eastern part of the district. In the central and western part the fluctuation ranges from 2- 3 m. (ground water department booklet of palakkad.)
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MATERIALS AND METHODS
3.1Data collection
Map representing respective points of measurements (observation well) (Fig.2) and the obserwation well data were
As we wanted to consider the spatial correlation among measured data and also the geostatistical method has been considered appropriate, Ordinary Kriging, has been selected as the interpolation method. For ordinary kriging the data series should have a normal distribution; otherwise the non-linear Kriging should be used or the data have to be turned into a normal distribution using convertor functions (M.I. Kamali et al 2015). The spatial correlation of the data is evaluated by semivariogram which is as follows
Fig 2. Semivariogram for average water level data
Fig 3. Semivariogram for minimum water level data
Fig 4. Semivariogram for minimum water level data
A semivarigram reveals the spatial structure of a variable and how it varies in different directions. In order to investigate geostatistical analysis and spatial correlation of the data, their semivariograms were calculated and different common semivariogram models (e.g., Spherical,Exponential, Gaussian and etc.) were fitted on them (M.I. Kamali et al 2015). In this study most preferable results were obtained by spherical model.spherical model defines mathematically as,
(h)=c(1.5 )+ when ha (1)
when h>a
where = is called the sill value, is the nugget effect (usually present) and a is the range or maximum zone of influence( Bernard Ofosu et.al. 2014).
To conduct geostatistical analysis GS+ software was used. For each model,Sill, Range and Nugget would be calculated. When the distance between the samples (h) increases, the value of semivariogram increases to a certain distance and then graph levels off which is called Sill (the model asymptote). The distance between the samples from which the variable values in adjacent areas have little effect on each other and with further increase the samples become independent, is called the Range or Radius of Influence. Also, the semivariogram value for h=0 is called Nugget. Ideally, theNugget should be zero, but in reality this status does not happen due to sampling, measurement and analysis errors of the data (M.I. Kamali et al 2015).
SE=0.196, nugget=0.2131, sill=0.43298,
range=39520.83,N/S index=0.496.
Fig 5 . Cross validation diagram for average water level data
SE=0.189, nugget=0.11257, sill=0.22580, range=32140,N/S index=0.501.
Fig 6 . Cross validation diagram for minimum water level data
SE=0.229, nugget=0.4176, sill=0.9736, range=20314.01,N/S index=0.571.
fig 7 . cross validation diagram for maximum water level data
Fig 8. Depth to ground water level diagram for average water level data
Fig 9 . Depth to ground water level diagram for minimum water level data
The N/S index is used to determine the correlation of the data. For N/S index values less than 0.25, between 0.25 and
0.75 and higher than 0.75, the spatialcorrelation is strong, moderate and weak, respectively (M.I. Kamali et al.2015)
-
RESULTS AND DISCUSSIONS
-
As it was mentioned, by using Ordinary Kriging interpolation method, the distribution function of the data was analyzed using GS+ software, then semivariogram values of the data were calculated and the best fitted models were determined. This was based on the Correlation of the data was investigated according to the Nugget to Sill ratio (N/S).Then the data were interpolated by Ordinary Kriging method.Then cross validation diagrams were plotted and the amounts of errors were calculated based on Standardized Error (SE).The depth to ground water level varies between
-
mto 9.98 m. The area including Cherpulassery, Vellinezhi, and Thchanattukara showed maximum water level in the maps and contain very little water. Based on this map the implication of ground water level on construction activities and civil engineering structures can be evaluated during preliminary stage of civil engineering projects.
ACKNOWLEDGMENT
We would like to express our thanks to ground water department, palakkad, for its corporation in the case study.
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Fig 10. Depth to ground water level diagram for maximum water level data