Jaipur Investment：Hydro Geochemical Factors Influencing The Dynamics of Grouper Characteristics in Eco-Sensitive Area Soft and Southern Western Ghats, India

The Results of Descriptive Statistics Analysis on the Quality Data are shown in Fig. 2. The PH of the Groundwater Ranged from 3.06 to 8.35, with Average E of 7.08, Suggesting that it is acidic to alkaline in nature (SI Table 1. StatisticsFor AnalySed Parameter). GROUNDWATER SAMPLES May Be Categorized As Acidic (PH 7.5, 44%, N = 25). GROUNDWATER SAMPLES with High Acidic PH Include S6 (3.06), S16 (4.40), S43 (4.00), S47 (4.10), And S48 (3.60). The lower phil. s, especially lateritic terrains like the samples aBove12, 132,22,24).EC Ranged from 50 to 970 μs/cm, with an average of 266 μs/cm. EC Fe Mn CA2+> Mg2+> K+ AND HCO3−> CL−> No3−> SO42−. SEDTo Investigate The HydroChemical Facies of the Study Region. The Chadha Diagram Reveals that the GROUNDWATER SAMPLES WERE Scattered Across Three Major Zones, W Its the exception of four samples. The samples have ben clustered together as follows: Cahco3 Facies (46%)> CAMGCL FACIES(30%)> NaCl Facies (17%)> NAHCO3 Facies (7%). The Facies of NaCl and CAMGCL of Grouper Show the Effect of ION Exchange PROTSSESSES, EVAPORATION ONEGED Storage/Residence But the Mineral Weathering Process IS only ExpectedTo have an impact on groupwater with cahco3 facies14,45. The Cahco3 Facies is observation in the Majority of the Samples from the district of Wayand, TTA, Palakkad and ThrisSur, and It Exhibitions The Recharging Water Features. FURTHERMORE, CAMGCL FACIES Indicate the ReverseION Exchange Properties of Water, As Found in the Majority of Samples from Distribes of Kazikhode, Malappuram, and Kottyayam. However, The NaCl Facies is Ly Seen in the Majority of Trivandrum Distribism.Ec. Subsequently, only four samples, Two from the IDUkki Distribution and Two from the Kollam Distribut, EXHibit Nahco3 Facies, Which is Indicative of the Base Ion Exchange Properties of the Water. Samples from the districts of IDUkki and Kollam Display Mixed HydroChemical Facies with An Asymmetrical Trend. Si Table 2(HydroChemical Facies Distribution) Displays The HydroChemical Facies Distribution.

To distinguish the influential hydrogeochemical projects in this aquifer, Gibbs and Bivar association plots we use.

Gibbs Employed the TDS and Ionic Ratios as a Means of Discerning The Primary Geochemical MechanisSMS that Govern the Chemical Composition of Water. and the anion plot (fig. 4A, B), The TDS is Plotted Against The Na++K+/NA++ K++ CA2+ Ratio and Against The Cl−/CL−+ HCO3− Ratio, Respectively. Evaporaning, Mineral Weathering, and Rainfall input May be Readily ED USING the Graphs. CA2+ and HCO3− Will Be Removed from the System During theProcess of Evaperation by Carbonate Precipity, Which Will the Be Followed by TDS Enrichment in the Aquifer45. AS A Result, The Concentrations of Na+ An CL− in G Roundwater Will Rise. In the Current Study, Around 10% of the Samples are Fall in PrecipitationZone and Rest of the Samples Cluster in a Zone of Mineral Weathering. No Samples are depicting on the event zone. recipition in the area of ​​study.

As Reported by Jankowski and ACWORTH23, The Plot of Ec Against Na+/CL− Will Not Change with Increasing Salinity (EC) IF Evaporab Hemistry. When na+/cl− is plotted aginst ec, as shown in fig.4C, only a FWLLS FOLLOW the TREND of Evaporation. This demonstrates that evaporation is not the dominant factor that information the Chemistry of Wate44. Figure 4C Shows. That the na+/clat ratios are enriched and dead, indicating that size dissation and the IonExchange Mechanism are primarily controlling the water checkry36,44.

IONIC RATIOS and BivAr asswelling in order to evacuate the carbonate disSOLUTION on Chemistry. Results of Carbonate Mineral DISS GROUNDWATER YIELD of CA2+, MG2+, and HCO3−33,44,46. In this Study, The Average CA2+/Mg2+ Molar Ratio Is 2.6, Which Varied from 0.19 to 9.7 ples (fig. 5). About 40% of theSamples have a CA2+/MG2+ Ratio Greater than 2. According to Maya and Loucks33, Dolomite DISSSOLUTION Will Retain A Ratio OF 1, whereas call dishereTion will re Sult in a Ratio Greater than 1. The Higher Ratio of CA2+/Mg2+ (> 2) isDue to Silicate Weathering in The System43,46Jaipur Investment. In the Present Study Area, Water Samples that are close to ca2+/mg2+ the = 1 line indicors that double disations, While Clusters that are between 1 and 2 Reveal that the disations of class.Existence of an IMPACT from Silicate Weathering in this aquifer is indicated by Higher Ratios, (CA2+/MG2+> 2).

AS Previously Stated, Silicate Weathering Influenced The Major Ion Chemistry in this aquifer43. FURTHERMORE, The Na+/CL− RATIO in this this aquifer Ranges from 0.05 to 3 .58, with an averaage of 1.45 (fig. 5). The dissation of haLite Will Maintain A1: 1: 1 Na+/CL n Ratio. However, The Weathering of Silicates and Cation Exchange Resulted in the System's System Sodium Content, Whit to a Ratio of Sodium To Loride Greater than One. In this study area, Art 81% ofSamples Indicate A Higher Ratio (Na+/CL−> 1), and the Sodium Content in theSese Wells is Obtaine, He Impact of Mineral Weathering and Ion Exchange Reaction, The Relationship Between CA2++ MG2+And HCO3 s+ SO42− is Exercised. If the CA2+ and MG2+ Result AS A CONSEQUENCE of the Weathering of Carbonate, SulPhate (GYPSUM, Anhydrite), and Silicate Miner ALS, then the HCO3−+SO42− Will Balance Both of Those Elements8, 34The Water Samples Plotted on or Near The 1: 1 Line in Fig. 5B Illustrate The Influence of Mineral Weathering on Water Chemistry in The Current Study. Samples Plot TED ABOVE Or Below the Equiline Indicate the Existence of Alternative Processses. Similarly, toInvestigate and distinguish the effects of Weathering of Silicates, Carbonates, and Evaporites/Evaporation in the Aquifer, Molar CA2+/NA+ Is Plotted Versus HCO3 n/NA+18,46. The Samples Wererbuted in A Cluster Between The EvaporabSilicate Weathering Zone, As Shown in Fig. 5. These Elements are mostly derived through. CREASE in Na+ Concentration in the Aquifers are explained by samples plotted on or near the evaporation zone. As a ResultOf the Weathering of Soda Feldspar (Albite), Potash Feldspar, Orthoclase, and MicroCline, Na+ and K+ Ions Are Released Into The Aquifer15,39.

CATION Exchange or Silicate Weathering are accountable for the Enriching of Na+ Over Cl−, While Reverse ION Exchange events are accountable for the depth of Na+ OVER E. The ION Exchange Process is Further Confirmed by the Plot of CA2++ MG2+ VS HCO3−++SO42n in Fig. 5b. The Presence of a High CA2++ MG2+ Concentration Over HCO3−+ SO42− in About 20% of the SAMPLES SUGGESTS A Reverse Process. CA2+ + MG2+ DepleTion Over HCO3−+ SO42− Confirms that CA2++MG2+ is withdrawn from groupwater by Cation Exchange Reaction or Na+/K+ Silicates Weathering Shior Increased HCO3−45. SimiLarly, The Ratio of Na+ +K+To HCO3− Demonstrates An Elevation of Na++K+in Relation to HCO3− AS A Result of CationExchange Activities (Fig. 5D). Schoellar, Described The Chloroalkaline IndoS (CAI 1 and CAI 2), Which WEEED in Several Studies to Elucidate ION Ge processes in groupwater50.

The Negative Values ​​of Cai 1 and Cai 2 Indicate Cation Exchange Process WHEREAS POSITIVE VALUES Indicate Reverse ION Exchange. VER CL− Result in Negative Values ​​in the Calculations, Indicating Cation Exchange Processses, whereas high connectrations of cl− overNA++K+Result in POSITIVE VALUES, Indicating Reverse ION Exchange Reactions. The Majority of the Samples (91%) Had Negative Values ​​and Show A Negative nd, as seen in fig. 5e. TheReface, CATION Exchange Reactions A Crucial Role in ControllingWater Chemistic, whereas only food is expina, T OF CA2++MG2+–alk – SO42− Versus Na++K+– Cl− Will Exhibit a Negative Slope anda significant neigatic correlation. Figure 5F DEPICTS A Negative Slope with A SIGNIFICANT Negative Correlation, Proving that Cational Exchange Reaction to min ERAL WEATHERING Influence the Water Chemistry in the Study Area.

Commonly, Aqueous Geochemical Calcurations are often use to exce exce examine the interactions? FICATION of Silicate Weathering and Carbonate Mineral Dissolution is Facilitated by THESE CALCULATIONS11. Determine the IonicStreingTh and Saturation Indices for Selected Minerals40,41. Ionic Streangth in the Current Study Ranged from 0.0009 to 0.014, With an Average Value of 0.004. Streangth has a significant correlation with ec as seen in fig. 6. FURTHER, The Average Valueof the partial presure of Co2 (PCO2) was found to be 2.88, and it ranged from − 9.24 to 0.03. At the local Ly Greater than the Atmospheric PCO2 (− 3.4),With the exception of Six Wells. Wells with More Salinity Water Have2 Higher Values, Which are Strongly Associated with the Atmosphere, and The Relationship BE Tween Ec and PCO2 Also Shows a Positive Tendency (Fig. 6). The PCO2 Numbers May Be Related toThe Grouper Level, and Deep Wells Tend to have low and pCO2. However, GROUNDWATER Level Data is not using to conformation for sampling wells.

According to si Calcurations and Fig. 6, About 20% of the GROUNDWATER SAMPLE WITH Carbonate Minerals SUCH AS CALCITE (CACO3), Aragonite (CACO3), Dolomi TE (CAMG (CO3) 2), SIDERITE (FECO3), and Rhodochrosite (Mnco3), indicating that disheres of carbonate minerals regulaters groupwater Chemistry. HCO3 a, as well as a neutral to alkaline ph, is further evidence that carbonate reactionHydrochmistic of the Grouper in Multilevel Wells. The Dolomite Saturation INDEX VALUES RANGE WIDELY ACROSS The Sample Wells (− 10.5 to 3.1). Bonate Minerals and their Wide Variation are cracial becaue group level variations in the sample wells may have caused Calcite andAragonite to Dolomitize as a Result of an interest with groupwater that contains magnesium.

GROUNDWATER Tends. UITable Thermodynamic Environment for the Precipition of Fe (III) PhasesFrom groupwater. Meanwhile, when fees (II) and Mn (II) Concentrations Increase, CORRESPNDINGLY Increases The Si of SiDerite and Rhodochrosite. Centrations in groupwater are constrained by adsorption OR Co-PRECIPITATION with Caco3, According to the Saturation of GROUNDWATER with Calcite, Sainterite, and Rhodochrosite5. On of Rhodochrosite37, 65. TheReface, These Minerals Have the Ability to Act as a Sink by Removing Fe (II) And Mn (II) ISS from Anoxic Grouper that contains a high concentration of HCO3−. Such processes can accelerate they Ced by Shifting The Equilibrium of Redox Towards The Reduced Phases of Fe Fe (II) andMn (II), Respectively.

Pearson Correlation Analysis was Performed in this Study and Results are presented in Fig. 8a. Variables namely ph. Tionally, PH Shows Significant Negative Correlation with No3− and K+. EC and Th Express Strong PositiveCorrelation with all variables except no3−, k+ and ph. No3− shows the significant correlation with only na+, K+ And CL− and Rest of the Parameter Are Nit with it whenas k+ shows correlation with only no3−.+ And K+ (R 2> 0.59) Suggest that Both are de derived from Anthropogenic SourceS in this aquifer. quifer. There are so42− are good indicator of anthropogenic input.− And so42d are partially or completely derived from anthropogenic source. Similarly, with the exception of pH, k+, and no3−, HCO3− Ve Correlation with all variables. Also, None of the Relationships Between The Concentration of Metals (Fe and mn) in Water Samples WeRe Significant. This Means that the Fe and Mn in the Water Samples WERE Not Related to OTHER PARAMETER and May And FROME FROME FROM DIFFERENT RCES in the Study Area.

One Effective Approach for Identifying the Origins of Variables and Geochemical Processs is the PCA Analysis. In PCA, The Water Analysis Data is reduced and and SIMPLIFIED Into Components. Tables 2 and 3 depicts the number of objects with eigen values ​​girl than one, as wellAs variance and Cumulative Variance. Similaly, A Graphical Illustration is Shown in Fig. 8BGuoabong Stock. In the Current Study, Three Factors Account for 77.1% of the Var InceSimla Wealth Management. Factor 1 has a substantial positive loading on Ec, Th, Na+, mg2+,CL−, HCO3n, and Anding, and It accounts for 50.2% of the variance. The main source of Chemical Constituents In this aquifer is mineral Weathering. ncludes gypsum and halite for the controling cl− and so42− in theaquafer. TheReface, Elevated HCO3− Loading Implies Those Processes. TheReface, Factor 1 value the impact of geogenic processes. Factor 2 accounts for 17.99.99.99.9 % of Total Variance and has a high positive loading of k+ and no3−. This factor Illustrates the Anthropogenic No3I Inflow Into This Aquifer. TheRe Is No Correlation Between No3− and CL−, SO42−, or Other Variables. Consequently In this aquifer. The Application of Frtilizers and Manures in Agricultual Practors Results inAn Incream Presence of No3− in GROUNDWATER DOE to Infiltration in the Vadose Zone. Factor 3, Which Accounts for 9.0% of the Total Variance, Exhibits POSITIVE Oadings only for and mn. This indicates that the lack of correlation between feelingOther Characteristics Suggests that their presence may be to the Weathering of Local Geological Formations Rich in theSerals, SUCH As Lalate and Archaean s.

The Results of HCA Presented in The Form of Polar Heat-Map (Fig. 8C) with Vertical DENDROGRAM (Q-MODE) RePRESENT The CLUSTER PARAMETERS and HORIZONTAL RAM (R-Mode) reply the cluster of sample local.Groups Shown in Q-MODE. Group 1 is associable with the elements EC, Th, Na+, Mg2+, CL−, HCO3−, and so42− , As Well As Gypsum and Halite, Are Prencent toa Certain extent. Group 2 consists of two variables. s Not Affected by Weathering or Anthropogenic Factors. Group 4 Includes Metals Like Fe and Mn, Which May Indicate A Potential Independent Origin Such as the Weathering of Laterite and Archaeans. Furthermore, in R-Mode, there are three clusters with 75% Samples ( n = 43) Fall Under Cluster 1, which is less mineralized, and the ECValues ​​with an Average of 160 μs/CM Which Suggest That Grouper is Located Nearby The Aquifer Recharge Area. Cluster 2 Accommodates 17% (n = 10) Samples with AV AV Erage of 470 μs/cm. This cluster indicates that waters that recladedLong AGO and have Fon A Certain Distance with the Aquifer Are Moderal Mineralized. E parts of IDUKKIDRICT. ONLY 4 SAMPLES (3 from Palakkad Distribu and 1 From Malappuram Distrib between)Cluster 3. GROUNDWATER in These Wells is Highly Mineralized and EC, with an Average Value of 900, Indicating High Mineralization.

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