Studies on the Textural Characteristics of Sediments from Vaigai River

INTERNATIONAL JOURNAL OF SCIENTIFIC & TECHNOLOGY RESEARCH, VOLUME 8, ISSUE 11, NOVEMBER 2019 ISSN 2277-8616 Studies on the Textural Characteristics of Sediments from Vaigai River Basin, Tamil Nadu, Southern India Arun TJ, Limisha AT, Krishna R Prasad, Aneesh TD, Sreeraj MK, Reji Srinivas*

Abstract— The sediment characteristics, in particular, the grain size distribution is important to be correctly determined for accurate representation in sediment transport to understand the source of evolution for sediments under the river environment. The present study illustrated the detailed textural variations in the sediments of Vaigai river basin, Tamil Nadu. The textural studies established clearly that the samples have insignificant fractions of finer grains, where sand and gravel were dominant. The textural nomenclature of the sediments mostly shows in the order sandy gravel - gravelly sand - slightly gravelly sand - muddy sandy gravel and slightly gravelly muddy sand. The statistical analysis of the samples was conducted in the study area; including the mean grain size, standard deviation (sorting), skewness and kurtosis. The sediments were dominant of course grain size, poorly sorted and very positively skewed. The kurtosis suggested dominantly leptokurtic nature of sediments. The statistical parameters display little temporal as well as spatial variations. The observations were supported by the polymodal nature of sediments that confirmed using the frequency distribution curves. At certain locations the unimodal and bimodal nature of the sediments were also present. The studied sediments are inferred to have deposited in quiet to calm environment. The energy process discriminate functions of the sediments were deposited predominantly as shallow agitated process under turbidity environment and remaining fluvial deltaic process. Based on the CM diagram, the debris transported under the tractive current thhrough rolling mechanism except a few samples that declined in bottom suspension and rolling. Furthermore, the anthropogenic interventions including the man-made structures like bridges and check dams in the fluvial system and the urbanized areas have a significant role in the overall dispersal pattern of sediments in the downstream of the rivers.

Index Terms— grain size distribution, Vaigai river, statistical parameters, frequency distribution curve, CM Pattern

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1 INTRODUCTION HE distribution of grain size has been widely used by the different energy conditions and extent of turbulence affecting T sedimentologist to elucidate transport dynamics as well as the environment [2]. The transport processes/ depositional to classify the sedimentary environment. The sediment mechanism of the sediments is reflected y the variations in the grain size will provide an indication of the shear stress to kurtosis [3,4,5]. Russell suggested that the size and shape will sustain and initiate the particle movements that must be promote the differential in entrainment, transport, and applied by the medium. They are closely related to the energy deposition of particles in sediments [6]. The homogeneity of of the medium that transports and the mode of transport. So the sediment mixture will influence the transport rate, where the sediment size that include the statistical size parameters the sediment is commonly being transported in individual size including the Graphic Mean (Mz), Inclusive Graphic Standard fractions [7]. The hiding effect or shielding of small particles Deviation (σi), Inclusive Graphic Skewness (Ski) and Graphic from the flow by larger particles in the non-homogeneous Kurtosis (KG) have been used to figure out the mechanisms sediment mixture resulted in varying fractions of transported during the deposition and transportation of the sediments, as sediment than their relative proportions in bed materials [8, 9]. well as to differentiate the various environment of deposition As the dynamics of sediments will act as transporting agents, in the recent as well as ancient sediments [1]. The difference in it plays an important role in environmental studies [10]. The the distribution of size and degree of sorting of grains is dynamics of sediments will produce changes in the mainly due to the variation in the energy of waves that parameters of grain size at the direction of transport and these reaching the sampling point, persistence and stability in trends have been widely used to regulate the dispersal pattern of sediments [11]. The variations in the fluidity factors and the ———————————————— energy seem to have an excellent correlation with the  Dr Reji Srinivas, Scientist, National Centre for Earth Science Studies, environment of deposition as well as its different processes Earth System Science Organisation, Ministry of Earth Sciences, [12]. So the studies on grain size will provide important clues Government of India, Thiruvananthapuram, India.-695011. E-mail: [email protected] to the depositional conditions, sediment provenance and  First author is currently pursuing PhD degree from CUSAT, Kerala, India. transportation history [13, 14, 15, 16]. In fluvial sediments, the E-mail: [email protected] determination of grain size distributions is a strenuous process. The depiction of the physical parameters in fluvial sediment mixture assists in the determination of local bed and

IJSTR©2019 www.ijstr.org INTERNATIONAL JOURNAL OF SCIENTIFIC & TECHNOLOGY RESEARCH, VOLUME 8, ISSUE 11, NOVEMBER 2019 ISSN 2277-8616 suspension loads to a high degree of certainty. The scrutinize of fluvial bed materials consent an identification of dominant sediment type in a particular river. Sand or gravel dominated fluvial sediments usually have varying range of grain size distributions. The studies on the textural characteristics of sediments have been subjected to intense research during the past few decades. In different environments, the textural characteristics of sediments have been studied by several authors [17, 18, 19, 20, 8, and 14]. Here an attempt is made to determine the texture, grain size distribution of sediments of the Vaigai river basin. 2 MATERIALS AND METHODS The samples were collected from the study area at each location using a stainless steel grab sampler and it transferred into a pre-labeled airtight container. The sampling using the grab will allow the collection of sediments including the sediments that transported along the bed and also the Fig. 1. Map of the Vaigai River Basin showing the sampling temporarily settled or trapped interstitially suspended locations materials among the bed load particles [21]. The samples were mixed thoroughly to make them homogeneous and a known quantity of samples was subjected to pre-treatment. The pre 4 RESULT AND DISCUSSION weighted samples were treated with dilute hydrochloric acid The textural analysis in the sediments from the study area of 0.2N and hydrogen peroxide of 30% to remove shell has been carried out to describe the spatial variation in the fragments and organic matter, as they interfere during the grain size characteristics of Vaigai river and the results are settling of particles. The pre-treated, samples were then presented in (Table 1). The collected samples from the Vaigai washed and dried at ~50˚C for further analysis. Textural river are composed substantially of gravel, sand, and mud. studies were carried out by standard sieving and pipette The grain size characteristics of sediment sampled from Vaigai analysis techniques followed by [22] and their statistical rivers are presented in (figure 2). Most of the sediment analysis following [23] was determined by using a samples from the study area are dominated by sand and modernized version of GRADISTAT software. gravel. In general, the Vaigai river exhibit the higher proportion of gravel (0% to 63%, with avg. 26%) and sand 3 STUDY AREA (35% to 93%, with an avg. 68%) with little percentage of mud The study area Vaigai River Basin, (VRB) is originating (3% to 24%, with an avg. 6%) respectively, towards the from the Sivagiri hills on the southern Western Ghats. The downstream direction. The textural classification after [25] for basins are advanced in the Proterozoic high-grade Southern gravel bearing sediments has been used to elucidate the Granulite Terrain (SGT) of Peninsular India, separated from textural nomenclature for the sediments of Vaigai river that the Archean low-grade Dharwar Craton to the north by the are furnished in the (Figure 3). The Vaigai river has mostly orthopyroxene isograd [24]. The Vaigai river basin (VRB) is sandy gravel - gravelly sand - slightly gravelly sand - muddy located between 9°15’ to 10°20’ N Latitude and 77°10’ to 79°15’ sandy gravel and slightly gravelly muddy sand. Spatially the E Longitude and spreads in the Theni, Dindigul, Madurai, coarser particles that dominate in the river channel are mainly Sivagangai, and Ramanathapuram districts (Figure.1). The due to the channel gradient and hard rock exposures within river is having a length of 258 kilometers with a drainage the river channel. So the variation in the granulometric basin of 7,031 square kilometers and the width varies from 6 to composition of the samples from Vaigai river can be related to 50 Km. It flows in the northeast direction through the the local geology or the slope characteristics. The study area Cumbam that lies between the Palani Hills to the north and shows some inconstancy in grain size composition. The energy the Varushanad Hills to the south. Finally, the river empties regime in the Vaigai river channel will continuously changed into the Palkstrait in Ramanathapuram District. The crystalline due to the construction of bunds across the river channel at hard rock masses of Archaean age on the western portion certain locations. The samples near these zones are forms the major part of the basin (74%) and the remaining characterized by low gravel content and a high amount of forms the sedimentary rocks of the upper Gondwana, Tertiary sand where the turbulence of water is comparatively lower. and quaternary age on the eastern portion (26%). The The sample locations (Vg 18 and Vg 16) 45 km and 65 km metamorphosed rocks such as cordierite, sillimanite bearing upstream from river mouth exhibit comparatively increased gneisses, quartzites, calc, gneisses and granulites will form the mud percentage as the sampling stations is located Archaean formations. downstream of newly constructed bunds where the energy regime changes and also due to the addition of considerable amount of finer clastics from the hinterland area during the

IJSTR©2019 www.ijstr.org INTERNATIONAL JOURNAL OF SCIENTIFIC & TECHNOLOGY RESEARCH, VOLUME 8, ISSUE 11, NOVEMBER 2019 ISSN 2277-8616 monsoon season. Vaigai river sediments were calculated and represented in From the sample sites of (VG10), there is a fining of (Table 2). sediments (sandy gravel to gravelly sand) are progressively abundant down the stream, as the river enters into the midland and lowland, where there is a change in physiography which in sequence are characterized by

TABLE 1 The textural characteristics of the sediments from Vaigai River Basin Sample Gravel Sand Mud Sediment Type No: % % % (Folk et al, 1970) VG S1 33.85 62.23 3.92 sandy Gravel VG S2 41.59 55.08 3.33 sandy Gravel VG S3 4.10 89.23 6.67 slightly gravelly Sand VG S4 25.36 71.41 3.24 gravelly Sand VG S5 43.62 53.35 3.03 sandy Gravel VG 1 25.51 70.59 3.90 gravelly Sand VG 2 38.26 58.44 3.30 sandy Gravel VG 3 21.91 74.55 3.54 gravelly Sand VG 4 26.18 70.14 3.68 gravelly Sand VG 5 40.09 55.21 4.71 sandy Gravel Fig.2. Showing the grain size distribution of sediments VG 6 47.12 49.34 3.54 sandy Gravel collected from Vaigai River basin VG 7 62.77 34.33 2.89 sandy Gravel VG 8 31.82 63.85 4.33 sandy Gravel VG 9 42.60 53.80 3.60 sandy Gravel VG 10 33.17 62.94 3.89 sandy Gravel VG 11 49.73 46.76 3.52 sandy Gravel VG 12 18.32 74.81 6.87 gravelly Sand VG 13 41.19 54.78 4.03 sandy Gravel VG 14 28.86 67.35 3.79 gravelly Sand VG 15 6.18 89.53 4.28 gravelly Sand VG 16 14.32 64.17 21.50 muddy gravelly Sand VG 17 3.62 91.22 5.16 slightly gravelly Sand VG 18 0.04 55.26 44.69 slightly gravelly muddy Sand VG 19 6.53 89.42 4.05 gravelly Sand VG 20 4.60 83.43 11.97 gravelly muddy Sand VG 21 3.09 90.04 6.87 slightly gravelly Sand VG 22 0.00 75.19 24.81 slightly gravelly muddy Sand VG 23 0.00 87.58 12.42 slightly gravelly muddy Sand fluctuating energy condition and varied granulometric composition. The decrease of phi mean towards the downstream and the gradual enhancement in the fining of sediment classes is influenced by the effect of abrasion and progressive sorting [13, 26]. Minor variations in sample Fig. 3. Showing the textural nomenclature after Folk and Ward (1970) of the Vaigai river basin, based on sand silt clay ratios characteristics may be related to the changes in the river bed characteristic. The variations in grain size population are also due to the effect of natural and manmade obstacles like meanders, check dams and bridges along the river course. The 4.1 Mean size (mz) conspicuous variation in the flow regimes is one of the The average size of the sediment in the spectrum of grain size innovative factors responsible for the noticed variation in the or the central tendency, which in turn displaying the index of textural peculiarity of the riverine sediments. In addition, the energy that impacted to the sediment due to the velocity of construction of check dams and bunds also influence the current and the turbulence of the medium of transport is drastic changes in the dispersal pattern of silt and clay in the termed as the graphic mean size [18, 20, 27]. The mean values sediment substratum. of the surface sediments of the Vaigai river sediments ranges The statistical parameters namely mean size, sorting, from (-1.085 to 8.169) with an average (0.701) falling in skewness, and kurtosis obtained from grain size analysis for

TABLE 2. A statistical overview of textural parameters of the sediments from Vaigai River Basin

Smpl Mean Size Stan Dev Skew Kurto Mean Size Stan Dev Skewness Kurtosis id: (Mz) (σI) (SkI) (KG) (Mz) (σI) (SkI) (KG) VG S1 -0.017 1.557 0.376 0.787 Very Coarse Poorly Sorted Very Fine Platykurtic Sand Skewed VG S2 -0.161 1.591 0.420 0.730 Very Coarse Poorly Sorted Very Fine Platykurtic Sand Skewed VG S3 0.823 2.087 0.296 3.449 Coarse Sand Very Poorly Fine Skewed Extremely Sorted Leptokurtic VG S4 0.210 1.499 0.147 0.811 Coarse Sand Poorly Sorted Fine Skewed Platykurtic VG S5 -0.534 1.187 0.408 0.979 Very Coarse Poorly Sorted Very Fine Mesokurtic Sand Skewed VG 01 -0.156 1.247 0.322 1.083 Very Coarse Poorly Sorted Very Fine Mesokurtic Sand Skewed VG 02 -0.475 1.138 0.305 0.910 Very Coarse Poorly Sorted Very Fine Mesokurtic Sand Skewed VG 03 -0.194 0.978 0.079 0.874 Very Coarse Moderately Symmetrical Platykurtic Sand Sorted VG 04 -0.018 1.304 0.126 0.814 Very Coarse Poorly Sorted Fine Skewed Platykurtic Sand VG 05 0.050 1.885 0.593 1.094 Coarse Sand Poorly Sorted Very Fine Mesokurtic Skewed VG 06 -0.404 1.526 0.527 0.825 Very Coarse Poorly Sorted Very Fine Platykurtic Sand Skewed VG 07 -1.085 0.807 0.391 1.475 Very Fine Moderately Very Fine Leptokurtic Gravel Sorted Skewed VG 08 -0.309 1.332 0.357 1.192 Very Coarse Poorly Sorted Very Fine Leptokurtic Sand Skewed VG 09 -0.426 1.431 0.460 1.110 Very Coarse Poorly Sorted Very Fine Mesokurtic Sand Skewed VG 10 -0.502 0.937 0.223 0.966 Very Coarse Moderately Fine Skewed Mesokurtic Sand Sorted VG 11 -0.668 1.155 0.484 0.901 Very Coarse Poorly Sorted Very Fine Mesokurtic Sand Skewed VG 12 0.258 2.360 0.421 2.090 Coarse Sand Very Poorly Very Fine Very Leptokurtic Sorted Skewed VG 13 -0.329 1.469 0.425 0.894 Very Coarse Poorly Sorted Very Fine Platykurtic Sand Skewed VG 14 0.320 1.699 0.198 0.763 Coarse Sand Poorly Sorted Fine Skewed Platykurtic VG 15 0.866 1.174 -0.188 1.190 Coarse Sand Poorly Sorted Coarse Skewed Leptokurtic VG 16 2.992 4.635 0.700 0.896 Fine Sand Extremely Very Fine Platykurtic Poorly Sorted Skewed VG 17 0.759 1.413 0.178 1.772 Coarse Sand Poorly Sorted Fine Skewed Very Leptokurtic VG 18 8.169 3.583 -0.530 0.798 Very Fine Very Poorly Very Coarse Platykurtic Silt Sorted Skewed VG 19 0.576 1.054 -0.055 1.338 Coarse Sand Poorly Sorted Symmetrical Leptokurtic VG 20 1.785 2.592 0.439 2.842 Medium Very Poorly Very Fine Very Leptokurtic Sand Sorted Skewed VG 21 1.000 2.118 0.332 4.607 Coarse Sand Very Poorly Very Fine Extremely Sorted Skewed Leptokurtic VG 22 5.011 4.212 0.657 0.734 Coarse Silt Extremely Very Fine Platykurtic Poorly Sorted Skewed VG 23 2.074 2.312 0.564 2.750 Fine Sand Very Poorly Very Fine Very Leptokurtic Sorted Skewed Index: (Mz) = Mean Size ; (σI) = Standard Deviation; (SkI) = Skewness; (KG) = Kurtosis

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(very coarse sand to very fine silt) with the average displays continues addition of coarser / finer sediments in the varying course sand (Figure 4). The variations in the phi mean size will proportion [18]. The mixed sediment transport towards endorse the appearance of energy condition in their median of downstream will causes a decrease in the sorting [13]. deposition and also the average kinetic energy of the depositing agent [14, 28, 27]. If the sediments become coarser then the phi mean size decreases and if the phi mean size increases then the sediment becomes finer due to the exponential transport mechanism that exists along the river flow stated by [29,30,]. So the distribution pattern of mean size in the study area generally demonstrates that the sediments were deposited under a moderately low energetic condition as well as the low fluvial discharge. The locations that have coarser sediments, will follow impeachment under the little distance of transportation, moderate to high flow and also the hard rock present in the catchment area [31,32,33]. The strong winnowing action of the coarser particles in the high energy surrounding will eliminate the fine sediments [18, 34, 35].

Fig. 5. Spatial distribution of Standard Deviation in the sediments of Vaigai River Basin

4.3 Skewness (SkI) The graphic skewness is an important parameter that measures the dissymmetric degree of the frequency distribution of either predominance coarse or fine sediments with respect to the median value [37]. The variation in the energy conditions of the sedimentary process is reflected by the skewness [38]. The inclusive skewness amount in the sediments of the Vaigai river ranges from (-0.530 to 0.700) with a moderate value of (0.309) declining (64%) very fine skewed, (21%) Fine Skewed, (7%) Symmetrical, (4%) very coarse Fig. 4. Spatial distribution of Mean size in the sediments of skewed and (4%) of Coarse Skewed nature respectively Vaigai River Basin (Figure 6).

4.2 Standard Deviation (σI) The uniformity in the distribution of particle size or the sorting that illustrating the accelerating conditions of the depositing agent or the fluctuations in the aggressive energy is measured by the graphic standard deviation [20]. The standard deviation values of the Vaigai river ranges from (0.807 to 4.635) with the moderate value of (1.796) indicating (moderately sorted to extremely poorly sorted) with the average falling poorly sorted nature. Around 61% declined in the poorly sorted, 21% very poorly sorted, 11% moderately sorted and 7 % extremely poorly sorted (Figure 5). Like mean size, there is also a change in the values of standard deviation towards the downstream direction, demonstrating the influence of mean grain size on the sediments sorting nature [29]. The variation in the turbulence of water and the variability in the velocity of the depositing current will be attributed to the fluctuations in the sorting values [36]. The Fig. 6. Spatial distribution of Skewness in the sediments of variations in the value of sorting are feasible as long as the Vaigai River Basin

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The selective removal of fine particles or the addition of maturity of sand and deviation in the sorting values due to the materials to the coarser debris of a normal population due to prolonged addition of coarser and finer materials in changing the winnowing action will exhibit the coarse skewness [39]. proportion [4]. The leptokurtic character exhibits the impact of The study area is exhibiting dominantly the very positively variation in the energy condition during the deposition of skewed nature. The deposition, as well as the unidirectional sediments [4]. transport of sediments at the environment that has the low energy, is revealed by the positive skewness whereas the 5 FREQUENCY CURVES negatively skewed sediments illustrate the deposition that Frequency distribution curves (FDC) are the smooth curves took place at a higher energy environment [13, 40]. The that represent the variation in the weight percentage of enormous riverine input will imply the very fine skewed different fractions within the sediments. The nature of the nature of the sediments. The changes in the flow pattern of the sediments can be illustrated through the FDC. The frequency river are reflected by the downstream variation in the values distribution curve of the Vaigai river samples is shown in of skewness [13]. (Figure 8). The frequency distribution curves illustrate that the majority of samples Vaigai river inferred the polymodal 4.4 Kurtosis (K ) G distribution. The sediments infer (50%) polymodal, (39%) The quantitative measure used to describe the departure bimodal and (11%) unimodal distribution. The peak of an from the normal distribution is the striking kurtosis. The incremental frequency curve is served as the mode. If a minimum and maximum values of kurtosis within the Vaigai particle size of sediment is domineering over the others in a river ranges from (0.730 to 4.607) with an average (1.381) sample, then it is termed as unimodal and the size-frequency implying (Platykurtic to Extremely leptokurtic) with moderate curve can be characterized by more or less distinct peaks. falling leptokurtic nature. The overall samples exhibit (39%) Those curves, that having two distinct peaks are termed as platykurtic, (36%) leptokurtic and (25%) mesokurtic nature bimodal and polymodal are those with more than two peaks. (Figure 7). The variation in the downstream direction of the The polymodal nature of the curve is mainly due to the kurtosis value is a reflection of the flow peculiarity within the extreme fluctuations in the velocity of the depositing agent or medium of deposition [3, 41]. The immaturity of the sand is the absence of certain grain size in the size range of source imitated by the very platykurtic nature in the sediments, due material [27]. The sediments were deposited after the different to the uninterrupted addition of finer/coarser materials in the modes of transportation such as rolling, sliding, saltation and fluctuating proportion by the tributaries by the variation in the suspension processes [44]. So the particles from different sorting values [13]. The mesokurtic to leptokurtic nature in the sources were imitated by the polymodal nature of the studied sediments of the study area is attributed to the unceasing samples. Further the fluctuations in the velocity of current admittance of well made or coarse grains after the scatter during the deposition of these particles will also exhibit the polymodal nature. 6 BIVARIATE PLOTS The interrelationship and trends displayed in the bivariate plots will demonstrate the mode of deposition and its following environments [44, 45 and 23]. The geological significance of the grain size parameters can be figure through the bivariate plots [46]. The bivariate plots of statistical parameters accomplished of Vaigai sediments are portrayed in (figure 9). The Mean size Vs Standard deviation (figure 9a) illustrates a linear relationship that the finer particles (particles with higher phi mean values) displays enhanced sorting i.e. the sediment size decreases as the sorting worsens. The Mean Vs Skewness (figure 9b) shows approximately a definite scatter pattern in the study area. The plots indicate the decrease in grain size with a positive skewed over negative skewed trend. The sediments of negative skewness ensure in Fig. 7. Spatial distribution of Kurtosis in the sediments of high energy environment and the positive skewness occurs Vaigai River Basin under the low energy environments [20]. The bivariate plots between mean and kurtosis (figure 9c) show a marginal rising action and equity of their original condition till the deposition linear pattern, reflecting the combination of coarser and finer [42]. The very leptokurtic nature of sediments demonstrate particles. The standard deviation Vs skewness (figure 9d) plot that the mixing of predominant population (finer materials) is is showing that sediments are coarsely skewed to very fine higher and the medium material is very low [43] or the skewed with extremely poorly sorted to moderately sorted

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VG S 01 VG S 02 VG S 03 VG S 04

VG S 05 VG 01 VG 02 VG 033

VG 04 VG 05 VG 06 VG 07

Weight % Weight

VG 08 VG 09 VG 10 VG 11

VG 12 VG 13 VG 14 VG 15

VG 16 VG 17 VG 18 VG 19

VG 20 VG 21 VG 22 VG 23 Phi Value Fig. 8. Showing the Frequency distribution curves of the sediments in different locations of Vaigai river Basin

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a b c

d e f

Fig. 9. Binary plots between various textural parameters of the sediments of Vaigai River Basin. (a) Mean vs. Standard Deviation (b) Mean vs. Skewness (c) Mean vs. Kurtosis (d) Standard Deviation vs. Skewness (e) Standard Deviation vs. Kurtosis (f) Skewness vs. Kurtosis. (Index: VPS - very poorly sorted, PS - poorly sorted, MS - moderately sorted, MWS - moderately well sorted, WS - well sorted, VFS - very fine skewed, FS - fine skewed, NS - near symmetrical, VL - very leptokurtic, LK - leptokurtic, MK - mesokurtic, PK - platykurtic, VPK - very platykurtic). behavior. The environment of deposition can be generally identified by using this plot [47]. The plot also describes the tendency of the skewness to increase towards the decrease in the standard deviation due to the action of the littoral currents [19]. The standard deviation and kurtosis (figure 9e) denote predominantly the increase of kurtosis value with increase in the standard deviation except a few sediments that exhibit the decrease of kurtosis with the increase of standard deviation. The skewness vs. kurtosis (figure 9f) plot lacks any pattern as there is a wide range of scattering of points. 7 SUITE STATISTICS Stewart, [48] has proposed a plot of the discrimination field to understand the energy process by using the bivariate plot of mean and standard deviation (Fig 10). The sediments of the study area were superimposed on the plot recommended by [48] and indicate that the majority of the Fig. 10. Energy Process based on Mean vs. Sorting (after sediments from Vaigai river basin were distributed in the Stewarts, 1958) for the sediment of the Vaigai River Basin field of river process except few in the inner shelf and quiet water environment. inclusive graphic standard deviation (sorting), 'Sk' serve as the skewness and 'KG' serves as the graphic kurtosis. 8 LINEAR DISCRIMINATION FUNCTION a) Discrimination between Aeolian and Beach environment (Y1) The linear discrimination function analysis within the 2 Y1 = -3.5688 Mz + 3.7016 ẟ1 - 2.0766 Sk + 3.1135 KG sediments was entrenched by [27] for interpreting the If Y1 is ≥ -2.7411, the environment of deposition indicates depositional setting by applying the following equations, Beach and Y1 is ≤ -2.7411, then the environment of where 'Mz' serve as the grain size mean, 'ẟ1' serve as the deposition implies Aeolian.

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TABLE 3 Showing the linear discrimination function (LDF) analysis in the sediments of Vaigai River Basin

Sl No: Y1 Remarks-Y1 Y2 Remarks-Y2 Y3 Remarks-Y3 Y4 Remarks-Y4 VGS1 10.706 Beach 180.422 Sh. Agitated water -23.048 fluvial(deltaic) 5.705 turbidity VGS2 11.342 Beach 184.819 Sh. Agitated water -24.227 fluvial(deltaic) 5.556 turbidity VGS3 23.313 Beach 368.294 Sh. Agitated water -39.208 fluvial(deltaic) 19.084 fluvial(deltaic) VGS4 9.790 Beach 168.677 Sh. Agitated water -20.314 fluvial(deltaic) 4.529 turbidity VGS5 9.320 Beach 109.689 Sh. Agitated water -14.442 fluvial(deltaic) 6.976 turbidity VG01 9.011 Beach 125.544 Sh. Agitated water -15.182 fluvial(deltaic) 7.162 turbidity VG02 8.685 Beach 99.954 Sh. Agitated water -12.920 fluvial(deltaic) 6.002 turbidity VG03 6.784 Beach 77.369 Sh. Agitated water -8.773 fluvial(deltaic) 4.634 turbidity VG04 8.629 Beach 128.770 Sh. Agitated water -15.478 fluvial(deltaic) 4.457 turbidity VG05 15.148 Beach 265.289 Sh. Agitated water -33.969 fluvial(deltaic) 8.388 turbidity VG06 11.533 Beach 171.456 Sh. Agitated water -23.051 fluvial(deltaic) 6.685 turbidity VG07 10.066 Beach 70.177 Sh. Agitated water -7.856 fluvial(deltaic) 9.392 turbidity VG08 10.639 Beach 140.230 Sh. Agitated water -17.317 fluvial(deltaic) 7.775 turbidity VG09 11.600 Beach 156.714 Sh. Agitated water -20.253 fluvial(deltaic) 7.836 turbidity VG10 7.583 Beach 71.711 Sh. Agitated water -8.874 fluvial(deltaic) 5.902 turbidity VG11 9.124 Beach 102.686 Sh. Agitated water -14.206 fluvial(deltaic) 7.008 turbidity VG12 25.326 Beach 416.324 Sh. Agitated water -50.679 fluvial(deltaic) 11.840 fluvial(deltaic) VG13 11.064 Beach 160.915 Sh. Agitated water -21.040 fluvial(deltaic) 6.488 turbidity VG14 11.501 Beach 212.282 Sh. Agitated water -26.117 fluvial(deltaic) 4.440 turbidity VG15 6.104 Beach 122.695 Sh. Agitated water -10.845 fluvial(deltaic) 5.103 turbidity VG16 70.170 Beach 1487.603 Sh. Agitated water -190.715 fluvial(deltaic) 2.957 turbidity VG17 9.832 Beach 179.147 Sh. Agitated water -18.068 fluvial(deltaic) 10.318 fluvial(deltaic) VG18 21.964 Beach 976.836 Sh. Agitated water -107.536 fluvial(deltaic) 1.374 turbidity VG19 6.337 Beach 105.769 Sh. Agitated water -9.232 fluvial(deltaic) 6.676 turbidity VG20 26.427 Beach 529.776 Sh. Agitated water -60.337 fluvial(deltaic) 16.575 fluvial(deltaic) VG21 26.698 Beach 401.801 Sh. Agitated water -40.435 fluvial(deltaic) 25.531 fluvial(deltaic) VG22 48.693 Beach 1269.446 Sh. Agitated water -157.141 fluvial(deltaic) 4.774 turbidity VG23 19.778 Beach 444.870 Sh. Agitated water -48.873 fluvial(deltaic) 17.693 fluvial(deltaic) b) Discrimination between the beach and the shallow the results from the present study indicate that the agitated marine environment (Y2) deposition of the sediments in this area was derived from Y2 = 15.6534 Mz + 65.7091 ẟ12 + 18.1071Sk + 18.5043 KG the fluvial environment (sediment discharged by the river). Here the Y2 ≥ 63.3650, the environment of deposition implies shallow agitated marine environment and Y2 is ≤ 9 HYDRODYNAMIC CONDITION 63.3650, then the environment of deposition indicates the The ternary diagram that mostly characterizes between beach. an aggregated fine fraction and non-aggregated coarse c) Discrimination between shallow agitated marine and fraction, to understand the hydrodynamic condition of fluvial environment (Y3) deposition [49]. The ternary diagram put forth by [49] has 2 Y3 = 0.2852 Mz - 8.7604 ẟ1 - 4.8932 Sk + 0.0482 KG been applied for the Vaigai river sediments to deciphering If Y3 ≤ -7.4190, the environment of deposition indicates the hydrodynamic dynamic condition of deposition that fluvial and Y3 ≥ -7.4190 the environment of deposition occurring in the river (Fig 12). Then the overall results implies shallow marine. reveal that the Vaigai samples exhibit a quiet to calm d) Discrimination between Fluvial and Turbidity (Y4) environment. 2 Y4 = 0.7215 Mz - 0.403 ẟ1 - 6.7322 Sk + 5.2927 KG If Y4 ≤ 10.000, the environment of deposition is fluvial 10 CM PATTERN and Y4 ≥ 10.000, the environment of deposition suggests The cm pattern was introduced by [45] to figure out turbidity. the hydrodynamic forces that occupied at the time of According to the linear discrimination function (LDF) impeachment of the granules. [45], explained the distinct analysis of the study area (Table and Fig 11), the values of pattern of cm plots in terms of different modes of Y1 falls in the Beach process. With reference to the Y2 values transportation by plotting the ' C ' i.e. coarser one percentile the whole samples fall under the shallow agitating process. value grain size in microns and ' M ' median value in The Y3 values indicate the fluvial environment. The Y4 value microns on log possibility scale. The CM pattern diagram shows that 78.57 % are turbidity environments and the perspectives an entire model of tractive current, which is remaining 21.43 % of Vaigai is the fluvial deltaic process. So

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sub divided into several segments such as NO, OP, PQ, QR and RS displaying different forms of debris convey. The segment NO represents the coarse grains transported by rolling, OP indicates the bottom suspension with rolling, PQ serves as the graded suspension no rolling while the QR parallel to the line C=M represents the main channel deposits and the RS the uniform suspension. The CM plot for the Vaigai sediments is shown in the (figure). The results show that most of Vaigai samples decline in the NO except few in the OP region. This field reflecting that most of the tractive current deposition by rolling mechanism while the few samples declined in bottom suspension and rolling. The cm pattern is illustrating the unfussiness of the hydrodynamic process operating in this system. The samples scattered above the ideal pattern indicate the complexity in the transportation regime which also reflects from the poorly sorted nature of these deposits.

Fig. 11. Showing linear discrimination function (LDF) analysis in the sediments of Vaigai River Basin

Fig.13. CM Pattern of the sediments of Vaigai River Basin

11 DISCUSSION The gradual downstream decrease in the grain size has been observed in the Vaigai river sediments. The Fig. 12. Hydrodynamic deposition of the sediments (after observation is exhibiting the geological presumption of the Pejrup, 1988) for the Vaigai River Basin grain size distribution that occurring in a tidal river during

INTERNATIONAL JOURNAL OF SCIENTIFIC & TECHNOLOGY RESEARCH, VOLUME 8, ISSUE 11, NOVEMBER 2019 ISSN 2277-8616 the downstream flow direction. The critical erosion velocity channel, meanders, the anthropogenic interventions that the sediments firm to motion is the minimum current including the man-made structures like bridges and check velocity to move the sediments of a particular size, the dams in the fluvial system and the urbanized areas may movement stops at lowest transport velocity and deposited also have a significant contribution to the change in the concede to the variation in the grain size with the heavier overall dispersal pattern of sediments in the downstream of ones deposited first and finer sediments come to rest as the the rivers. The pronounced impressions of the longitudinal current velocity decreases [50]. Hence the relationship profile of the river channel could force a more expeditious between the distribution of grain size and current velocity decrease in the deposited material [59]. So the minor in the Vaigai river, fining downstream sediments can be fluctuations in the grain size population if any in the study described as the current velocity which is high upstream areas may also be attributed to these factors [13, 60]. where the coarse grains remains and the decreased downstream towards the river mouth where the current 12 CONCLUSION energy is low. As the velocity increases in the upstream of The present work exhibits the nature of distribution in the river channel the more and more grains in the fine the grain size along the Vaigai river basin. The sediment individuals in the particle spectrum are appropriated and samples collected at the Vaigai river basin show that the will be selectively removed downstream. This study also fluvial bed materials are dominated by sand and gravel, agrees with the general rule after [51] for the mean grain indicating a homogenous sedimentary environment. Most size of sediments to the decrease in the current flow of the samples have significant fractions of sand and gravel direction. whereas finer grains of silt and clay have a minimal The distribution of clastic sediments in the rivers is percentage, except for the sediment collected near the river controlled by the hill slope process and the channel process. mouth. The statistical parameters, which including the The gravity of the sediments is controlled by the hillslope mean size, standard deviation, skewness, and kurtosis were processes and feasible to the river channel are through the evaluated in the study area. The textural parameters overland flow, the various mass movement mechanism and indicated that the sediments were very coarse sand to very the dissolution through the rain. Within the river channel, fine silt, moderately well sorted to poorly sorted with the natural factors such as bedrock outcrops, tributaries, dominantly very positively skewed and platykurtic to and terraces that inserting materials that have the extremely leptokurtic nature. The variation in mean size in characteristics enact individually of processes will be the study area is indicating the fluctuation in the energy negotiated longitudinally [52, 53]. Depending on the condition of the depositional environment at different hydraulic conditions and velocity within the channel, the locations. This is also reflected in the variation of standard materials that engender through these processes and the deviation from poorly sorted to moderately well sorted assign of sediments from upstream tributaries/channels will which might be attributed to the addition of finer materials move through the river channel. The channel processes will to coarser material in varying proportions at different control the deposition and transportation of the sediments locations. The Frequency Distribution Curves (FDC) clearly [54, 55, 56]. suggests that the sediments were dominantly polymodal The sand percentage in the study area was and bimodal in nature. The hydrodynamic condition comparatively higher within the freshwater region as ternary plot indicates that sediments were deposited under compared to the river mouth. The possible reason to quiet to calm environmental conditions. The energy process explain this difference is that the abrupt rivers will allow of discriminate functions illustrated that the sediments only the fine sediments to deposit, but after reaching the were deposited predominantly as the shallow agitated river mouth this flow is diminished dreadfully and process under turbidity environment and remaining fluvial allowing more fine sediments to be deposited. Also, the deltaic process. The CM pattern diagram illustrated that the tides have a momentous role in transporting offshore sediments sustain mostly tractive current deposition by sediments onto the river mouth, thus the offshore materials rolling mechanism except the few samples that declined in that subsisting of mostly fine sediments would also be bottom suspension and rolling. transported into the river but only little would reach further upstream due to the opposing river current [57]. The 13 ACKNOWLEDGEMENT decrease in the velocities of the ebb-tidal currents and the We would like to thank the Director, National Centre for occurrence of flocculation or the impact of the flood tidal Earth Science Studies (NCESS), Thiruvananthapuram, for dominant current and density current by salt wedges his support and providing facilities to conduct this resulting in a wide distributional area with very fine grain research. sediments [37]. 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