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Balashikha is the largest city in Moscow Oblast , Russia .

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Balashikha was founded in 1830, and became the center of the textile industry, but that is now closed

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From the Kursk railway station (Kurskaya and Chkalovskaya stations) in Moscow, trains leave for the Balashikha station (41 minutes).

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• Sports and ski complex "Lisya Gora" , Razinskoe highway, 69 , ☏ +7 495 521-81-18 , + 7-985-210-09-06 . W-Su 10:00 - 17:00 . ( updated Oct 2021 )

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The Composition and Element’s Speciation in the Spring Waters of the Southern Part of the Balashikha Urban District (Moscow Region)

• Published: 07 October 2023
• Volume 78 , pages 423–436, ( 2023 )

INTRODUCTION

Springs are specific natural formations that play a significant role both in feeding rivers and as sources of potable water for inhabitants. Within the bounds of urban agglomerations, the pollution of spring-feeding groundwaters is an urgent problem.

At the Moscow agglomeration, about 1000 springs are located including un managed ones and the areas of scattered discharge of groundwaters (Balabanov, Smirnov, 2006; https://riamo.ru/ ; Shvets et al., 2002). Springs are integral parts of urban landscapes with drainage areas subjected to pronounced anthropogenic impacts. Analysis of the ecological and hydrogeologic conditions of the formation of spring runoff along with water quality is a topical problem in the environmental studies. However, these springs (excluding individual cases) are not included in the Russian State Water Register or in the monitoring system of surface waters. In view of this, studies within the integrated studies in geologic engineering, hydrogeology, and geochemistry along with those aimed specially to inventory springs and to examine the formation conditions and water quality in springs are of special importance (Zeegofer et al., 1991; Shvets et al., 2002; Balabanov and Smirnov, 2006; Vasil’eva, 2009; Savenko et al., 2020).

The present study was aimed at determining the major and trace component compositions, along with occurrence forms of individual trace elements in the spring waters of the Balashikha urban district.

The considered area is situated on the Pekhorka River and borders Moscow on the west and Lyubertsy, Ramenskoe, Noginsk, Shchelkovo, Pushkino, and Mytishchi districts of Moscow Region on the south, east, and north, respectively. In a similar manner to all the cities of Moscow Region bordered by the Moscow Automobile Ring Road (MARR), Balashikha is permanently subjected to negative impacts from Moscow, in addition to quite powerful sources of environmental impacts. It is this area where the bulk of Moscow industrial emission to the atmosphere occurs, as well as where the sites of municipal and domestic waste burial are located and the wastewaters of the Moscow sewage waters flow. The combination of aquatic problems in the area, including the maintenance of surface and ground water quality, has a significant place.

A major part of the treated area is occupied by urban forest zones: Kuchino, Saltykovka, , and others. Within the city bounds, two well-known estates (Gorenki and Pekhra–Yakovlevskaya) are situated along with regional natural monuments (the parks in Poltevo and Novyi Milet villages). The high population density along with numerous transport junctions, industries, and other institutions result in the need to permanently solve the problems of the preservation of environment and natural aquatic formations. For this purpose, the development of a system of protected areas within the bounds of Balashikha urban district is designed. The development of protected areas includes integrated environmental investigations, the setting of required documents, appropriate agreements, and obligatory environmental expertise (Budarina et al., 2015). Among the places of interest of the area is the Lis’ya Gora alpine skiing complex, which is an anthropogenic landscape formed by the filling of the left bank of the Pekhorka River with foundry wastes. A subject may negatively affect the pedo- and hydrosphere of adjacent areas (Zaikina et al., 2012). The treated area includes two large waste burial sites (Purshevo and Kuchino), which have been revegetated by now ( http://www.balashiha.ru/ ; Fisun, 2018), as well as the inoperative Rusavkino quarry at the right bank of the V’yunka River near the outskirts of Novyi Milet village. (The quarry uncovers limestones and dolomites of the Upper Carboniferous Kasimov and Gzhel stages.)

The considered area is situated in the northeastern part of the Meshchera lowlands and is an eastward-sloping plain. In terms of hydrogeologic zoning, the area is located within the bounds of the Ucha–Balashikha hydrogeologic block associated with the western part of the Meshchera hydrogeologic region of the Moscow artesian basin.

The quaternary sediments include the following water-bearing layers: the present alluvial layer (a III kl); the locally slightly water-bearing Mikulino–Kalinin lacustrine–marshy layer (l,b III mk-kl); the water-bearing Moscow aquatic–glacial layer (f,lg II ms); and the water-bearing Don–Moscow aquatic–glacial layer (f,lg I ds-II ms). The Jurassic and Cretaceous sediments are characterized by the Neocomian–Aptian (K 1 nc-a) and Volga (K 1 nc-a) water-bearing complexes, as well as waters of sporadic occurrence in the Bathonian– Callovian sediments (J2bt-k) ( Geologicheskaya …, 1975).

The retaining Jurassic terrigenous layer is characterized by universal occurrence and subdivides the hydrogeologic section into two separated systems that show no hydraulic association with each other (the water-bearing layers in the Mesozoic and Cenozoic deposits and those in Paleozoic deposits). The top occurrence depth of Jurassic clays varies from 5 to 25 m. According to the large-scale mapping of hydrogeologic conditions over Moscow and Moscow Region performed by the specialists of the Institute of Geoecology, Russian Academy of Sciences (Pozdnyakova et al., 2012), the whole water-bearing mass overlying the Jurassic clays is commonly combined into the Over-Jurassic water-bearing formation. Below the Jurassic clays, the Upper- and Lower-Gzhel water-bearing layers (C 3 g 2 and C 3 g 1 , respectively) are situated, which are used as sources of potable water supply for the cities of Moscow Region.

MATERIALS AND METHODS

In September 2021, 12 springs of Balashikha urban district were tested ( Table 1 , Fig. 1 ). In the course of field surveys, the positions of springs were registered using a Garmin eTrex 10 GPS receiver, the spring discharges and temperatures were measured, as well as pH values and conductivity were determined with a portable PH 200 pH meter and a COM–100 conductometer (HM Digital Co., South Korea). To determine anion concentrations and oxidability (the chemical oxygen demand, COD), the water samples were collected with closable polyethylene vessels. To obtain the concentrations of major cations and trace elements, the samples were filtered through sterile filtering mount pieces of cellulose acetate of 0.45 μm pore diameter (CHROMAFIL Ca 45/25 S, Macherey–Nagel Co., Germany) to 15-mL test tubes of polypropylene and the filtrate was acidified to pH < 2 with extra pure HNO 3 .

The location scheme of spring sampling sites in the south of Balashikha urban district: ( 1 ), anthropogenic subjects with nos.: waste burying sites ((1), Kuchino; (2), Savvino; (3), Purshevo; (4), Torbeevo); quarries (5), Kupavna; (6), Rusavkino); technogenic mounds (7), Lis’ya Gora alpine skiing complex); ( 2 ), tested springs with nos.; ( 3 ), boundary of the southern part of Balashikha urban district, Moscow Region.

The concentrations of major cations (Ca, Mg, Na, and K) and trace elements (Sr, Ba, Fe, Mn, Co, Ni, Cu, Zn, Cd, Pb, Al, Ti, Rb, U, V, Cr, As, Se, Mo, P, and Ag) were determined using mass spectrometry with inductively coupled plasma (ICP–MS) with an ELAN 6100 mass spectrometer. The multielement standard solutions were used for calibrating (the ICP–MS 68 A, B set, High Purity standards, United States). The measurements were verified using the inner standard (Indium ICP Standard CertiPUR, 1002 mg/L ± 0.4%, Merck Co., Germany). The accuracy was controlled by measuring the CRM–TMDW standard solution (Trace Metals in Drinking Water Standard, High Purity Standards, United States).

The concentrations of Cl – and HC \({\text{O}}_{3}^{ - }\) ions were evaluated by volumetric titration; N \({\text{O}}_{3}^{ - }\) and N \({\text{H}}_{4}^{ + }\) ions were determined by potentiometry; to determine S \({\text{O}}_{4}^{{2 - }}\) ions, X-ray fluorescence analysis was used with previous concentration by the dried-drop procedure (Lubkova et al., 2022). The concentrations of P \({\text{O}}_{4}^{{3 - }}\) ions were calculated using the data on phosphorus determination in the samples by the ICP–MS technique. The COD value was determined by dichromate oxidability with photometric indication (a Portlab 501 spectrophotometer, United Kingdom) (GOST 31859–2012).

Based on the obtained analytical data, the thermodynamic calculations were performed for the dissolved occurrence forms of trace elements (Ba, Sr, Fe, Mn, Zn, Cd, Ni, Co, Cu, and Pb) in the waters. The Visual MINTEQ software was developed at the Royal Institute of Technology (Stockholm, Sweden) ( https://vminteq.lwr.kth.se ). Four types of databases are commonly used for the calculations: the database for individual components, the primary base of thermodynamic data, the database for solid phases, as well as that for the Gaussian model of complexation with a dissolved organic substance. The authors used for the calculations the Comp_2008.vdb, Thermo.vdb, Type6.vdb, and Gaussian.vdb databases, respectively. Owing to the permanent upgrading of the software, the sets of thermodynamic constants used with these built-in bases agree with each other and allow one to obtain reliable results.

The initial composition of the system was prescribed by the results of chemical analyses ( Tables 2 and 3 ). In this case, the DOC parameter (dissolved organic carbon) required for calculating the complexation with organic substances according to the Gaussian model of dissolved organic matter (Gaussian DOM) was calculated as DOC = 0.375COD where 0.375 = M(C)/M(O 2 ) = 12/32. In particular, this approach is commonly used in the studies of the Karelian Research Center (Lozovik et al., 2007).

The graphic presentation of major component composition of the waters used the diagrams by Stiff and Piper (Piper, 1944; Stiff, 1951) plotted using the GSS module of The Geochemist’s Workbench (GWB) software as the GWB Community Edition [ https://www.gwb.com ] free version.

RESULTS AND DISCUSSION

According to the geological and hydrogeologic maps at the 1 : 200 000 scale (sheets N-37-II and N-37-III), as well as to the explanatory notes for these maps ( Geologicheskaya …, 1975; Gosudarstvennaya …, 2001), the tested springs drain various water-bearing layers: the Kalinin alluvial layer ( n = 2), the locally slightly water-bearing Mikulino–Kalinin lacustrine–marshy layer ( n =1), the Don–Moscow aquatic–glacial layer ( n = 4), the waters of sporadic occurrence in the Bathonian– Callovian deposit ( n = 1), and the Upper-Gzhel water-bearing layer ( n = 1).

The data on major elements composition of spring waters are presented in Table 2 and in Stiff diagrams representing the equivalent composition of water for each of the sampling sites ( Fig. 2 ). The composition of dissolved forms of trace element is given in Table 3 .

The major component composition of spring waters (Stiff diagrams). Based on the geologic scheme of Quaternary deposits of the treated area; plotted by ( Geologicheskaya …, 1975; Geologicheskaya …, 1998; Gosudarstvennaya …, 2001). ( 1 ), lacustrine and marshy sediments, peat, peaty loams, sapropels (to 6–8 m); ( 2 ), alluvial deposits of flood plains, gravel- and pebble-containing sands, loams, and sandy loams, peaty in places (to 20 m); ( 3 ), Mikulino layer–Valdai superlayer, lacustrine–marshy deposits, clays, loams, and sandy loams interbedded with peat and sand (to 16 m); ( 4 ), Monchalovo–Ostashkov layers, alluvial deposits of the first fluvial terrace, sands, loams, and sandy–gravel deposits at the basement (to 16 m); ( 5 ), Kalinin layer, alluvial deposits of the second fluvial terrace (to 8 m); ( 6–10 ), Moscow layer: ( 6 ), alluvial–fluvio-glacial deposits of the third fluvial terrace (the region of Moscow Glaciation), sands, and sandy loams (to 6–10 m); ( 7 ), aquatic–glacial deposits of the time of deglaciation, sands, sandy loams, and loams (to 14 m); ( 8 ), aquatic–glacial deposits of the time of maximum expansion of glacier, sands, sandy loams, and loams (to 12 m); ( 9 ), glacial deposits: basal moraine containing gravel, pebble, and boulders, outliers of Prequaternary deposits (5–25 m, sometimes to 40 m); ( 10 ), glacial deposits: terminal moraine, boulder loams, sands, boulder–pebble sediments (to 40 m); ( 11 ), Likhvin layer, lacustrine and marshy deposits, clays, loams, and peat (to 9 m); ( 12 ), Don–Moscow layers, undissected complex of aquatic–glacial, alluvial, and lacustrine deposits, sands, sandy loams, and loams (to 12 m); ( 13 ), Muchkapsky layer. Roslavl series. Lacustrine and marshy deposits. Sands, clays, and peat (to 10 m); ( 14–15 ), Don layer: ( 14 ), aquatic–glacial deposits of the time of deglaciation, sands, loams, and clays (to 27 m); ( 15 ), glacial deposits: basal moraine; boulder loams with sand lenses and outliers of Prequaternary and quaternary rocks (commonly to 10–20 m, to 44 m in places); ( 16 ), Prequaternary deposits; ( 17 ), springs of water sampling; ( 18 ), key hole for plotting the geologic profile of Quaternary deposits; ( 19 ), boundary of Upper-Gzhel water-bearing layer; ( 20 ), boundary of the southern part of Balashikha urban district (Moscow Region).

As a result of the generalization of the data on major component composition, the classification Piper diagram was plotted (Piper, 1944). The variation in the cation compositions of the waters of drained layers are insignificant; the waters are mainly calcic and magnesium–calcic, excluding the calcic–sodium waters of the Kalinin Alluvial layer. The widest variations are characteristic for a anion composition of waters ( Fig. 3 ).

A Piper diagram for the major element composition of spring waters in Balashikha urban district by (Piper, 1944). The waters of spring 6 contain nitrate ion among the major components; its content is not included in the diagram plotting.

Springs 5 and 5a drain the waters of the Kalinin layer of alluvial deposits of the second fluvial terrace consisting of the sands and pebble at the basement, sometimes interbedded with loam. The waters are subacidic near-neutral (pH 6.3), 0.58–0.67 g/L mineralization, chloride calcic-sodium. According to the studies (Pit’eva, 1983; Vsevolozhskii, 1983), an atypical water composition for Quaternary deposits may be caused by upward discharge of deep-seated saline groundwaters of Late Devonian age.

The waters pf spring 6 are subacidic (pH 5.3), ultrafresh ( M 0.13 g/L), nitrate–sulfate calcic. According to the map of Quaternary deposits (sheet N-37-II), the lacustrine–marshy deposits of Middle and Upper Neo-Pleistocene are embedded as isolated lenses under the deposits of the Moscow moraine associated to the outflow of this spring. The authors assume that the spring drains the waters of the locally slightly water-bearing Mikulino–Kalinin lacustrine–marshy layer. This is supported by the fact that the waters of marshy deposits commonly contain considerable amounts of ammonium ion and hydrogen sulfide oxidizing to form nitrate and sulfate ions. Thus, nitrates in the spring water are most probably of a natural origin.

Springs 4, 7, 7a, and 9 drain the Don–Moscow aquatic–glacial water-bearing layer which occurs universally, lies at the Upper Jurassic regional impermeable layer, and is overlapped with the deposits of the Moscow moraine. The water-bearing rocks are presented by sands along with small pebbles and gravel, showing various degrees of clayiness. The filtration characteristics range from hundredths to 4.0–12.7 m/day. The waters are neutral (pH 6.6–6.9) sulfate–hydrocarbonate calcic. One must note that the water-bearing rocks are ferruginized at the point of the spring 7a outflow and the waters are considerably less mineralized compared to those of spring 7. The authors assume that the water composition at this outflow is formed under the inflow of the waters of sporadic occurrence in the Bathonian–Callovian deposits. These waters are discharged onto the surface as the upward spring 8. The waters are neutral (pH 6.7), ultrafresh ( M 0.15 g/L), and sulfate–hydrocarbonate calcic. The characteristic feature of the waters is high iron content of 6.4 mg/L according to the authors’ data ( Table 3 ) and 6 mg/L according to ( Geologicheskaya …, 1975), which is caused by the presence of pyrite inclusions and carbonaceous insets. The deposits of this layer are commonly constituted by fine-grained water-containing sands and are usually passed with no testing during the well drilling, recovered with pipes, and not exploited since layer waters that mix with those of the Carbonaceous layer may decrease the potable quality of waters.

The outflows of springs 1, 1a, and 2 are associated to the occurrence areas of the Volga deposits (sheet N-27-II) and the waters drain the Volga water-bearing complex. The results of analyses showed that the waters were subacid (pH 5.5–6.0), sulfate–chloride (or chloride–sulfate) sodium–calcic and are characterized by mineralization of 0.35–0.56 g/L. According to ( Geologicheskaya …, 1975), the water composition in the Volga layer is quite variable: hydrocarbonate, hydrocarbonate–sulfate, and chloride–sulfate waters are found, along with calcic, calcic–magnesium, and calcic waters in terms of cations. The water-bearing complex is used as springs and wells by the habitants for potable and domestic needs.

The waters of the upward spring 9a most probably drain the Upper-Gzhel water-bearing layer with contours over this area shown (according the hydrological map, sheet N-37-III) as those located below the first water-bearing layer from the surface. The waters are near-neutral (pH 6.8) of 0.61 g/L and sulfate–hydrocarbonate–chloride calcic.

The comparison of the obtained data on water ion composition with the fund materials (Geologic, 1975) in general shows their agreement ( Table 3 ). We note that a wide variability is characteristic of the ion composition of water-bearing layers determined by the surveys on hydrologic conditions in the course of the hydrogeologic mapping.

The springs are mainly discharged along the banks of the Pekhorka (nos. 1, 1a, 2, and 4) and Gorenka rivers (nos. 5, 5a, 6, 7, and 7a). The comparison of the obtained data to those on the major component composition in the Gorenka River for 2006–2009 (Maidzhi, 2011) and in the Pekhorka River for 2020 (Novikov, 2020) showed that the composition of riverine waters was similar in general to that of the springs. The main distinctions were registered for nitrate and ammonium ions, showing 2- to 4-fold concentrations in springs compared to riverine waters. Despite the increased contents, the concentration of nitrate ion in spring waters is below the maximum allowable values for potable waters (45 mg/L) (SanPin 1.2.3684-21). An ultra-high content of ammonium ion (over 1.5 mg/L) was found in the waters of the Kalinin alluvial and Volga water-bearing layers (1.6–4.7 mg/L).

The concentrations of the majority of the considered trace elements ( Table 4 ) are within the range characteristic for groundwaters in the leaching zones of a temperate climate (Shvartsev, 1998) and conform in general to the average contents in surface watercourses to which they are discharged (Gaillardet et al., 2014).

The minimum variabilities (by factors of 2–5) are characteristic for the concentrations (μg/L) of Pb (0.11–0.22), Al (30–90), Ti (1.11–3,48), Cr (0.6–2.0), Ag (0.02–0.07), Cu (1.13–4.51), Zn (3.2–15.1), Rb (0.74–4.33), and As (0.48–2.91). Variations by factors of 10–20 were found for Ba (11–92), Sr (93–1300), Co (0.11–1.94), V (0.18–3.39), Se (<0.05–1.03), and Ni (0.8–17.4); the concentrations of Mo (0.03–1.95) and Cd (<0.01–0.35) varied by factors of 50–100. Despite the considerable variations, the contents of trace elements do not exceed the TLV for potable waters (SanPiN 1.2.3684-21), which points to the absence of any pronounced groundwater pollution in Balashikha urban district.

The widest variations of the concentrations in spring waters were found for Fe, Mn, and U. The content of iron varied within 31–6740 μg/L. The maximum values were characteristic for the waters of sporadic occurrence in the Bathonian–Callovian deposits (spring 8), which was caused by pyrite inclusions within the water-bearing deposits and by anoxic conditions of the formation of groundwaters characterized by the divalent state of iron. In the case of direct collection from the spring, the water was transparent, with no turbidity and color change. However, divalent iron is oxidized under the action of air and precipitated as reddish–brown sediment of the oxides and hydroxides downstream of the site of the spring outflow. The content of iron at the instant the sample was collected from the spring pronouncedly exceeds (by over 20 times) the TLV for potable water (SanPiN 1.2.3684-21). However, resulting from the oxidation and precipitation of iron, the concentration of Fe in dissolved form decreases even during a day to 189–200 μg/L, which is below the prescribed values. The concentrations of iron in the waters of other springs are quite similar (31–349 μg/L). A moderate exceedance of the TLV for potable waters (by a factor of 1.2) was found in spring 2 draining the Volga water-bearing complex. We note that the hydrochemical anomalies of dissolved iron (and manganese) forms with TLV exceedance are registered at times in several springs of the Moscow region (Shvets et al., 2002; Savenko et al., 2020). Iron in water belongs to the III class of hazard (moderately hazardous substances); the TLV is estimated by organoleptic parameters of adversity (the odor, color, and taste). It should be emphasized that the World Health Organization (WHO) has proposed no standard for iron, but it is stated that a value below 2 μg/L constitutes no health hazard ( Guidelines …, 2017).

The manganese concentration in spring waters varied within a wide range (0.8–299 μg/L). As one of the most abundant metals in the Earth’s crust, manganese is usually accompanied by iron. The increased Mn content (143 and 171 μg/L) which moderately exceeds the TLV of potable water (by 1.7 times) was registered in the water of springs 2 and 8, which were characterized by the maximum iron concentration, as noted. The absence of increased concentrations of other toxic metals points to a natural source. The waters of the Don–Moscow aquatic–glacial water-bearing layer are the most irregular in the content of this element. The maximum Mn content of 299 μ/L exceeding by three times the TLV was registered in the water of spring 7 draining this water-bearing layer. The spring is located nearby the Lis’ya Gora alpine skiing complex, which was built using foundry wastes. The soils in this area showed an increased content of manganese (Zaikina et al., 2012). We note that, similarly to iron, manganese belongs to the III class of hazard (moderately hazardous substances); the limiting parameter of adversity is organoleptic. The increased manganese content adversely mainly affects the conditions of the main water pipes owing to the formation of sediment of oxides within the distribution system. The standard sanitary value for manganese calculated by the WHO starting from the top limit of the range of the element supply is 0.4 mg/L ( Guidelines …, 2017), which is higher than the values in the water of the tested springs.

The maximum variability (over three orders of magnitude) occurs for uranium (0.01–14.7 μg/L). An increased U content is registered in the water of spring, draining the Upper-Gzhel water-bearing layer. The concentration of uranium does not exceed the TLV for potable water (15 μg/L) and is far below the standard value of the WHO of 30 μg/L ( Guidelines …, 2017).

The results of thermodynamic calculations for dissolved occurrence forms of trace elements are presented in Fig. 4 . The bulk of the Ba, Sr, and Fe (over 90%) occurs in solution as free ions. The distribution of other elements by occurrence forms is considerably affected by the anion composition of the waters. Free ions are more characteristic as well for Mn (91–96%), Co (86–95%), Ni (81–92%), Zn (86–94%), and Cd (68–94%). The sulfate–hydrocarbonate waters of the Don–Moscow and Upper-Gzhel layers at near-neutral pH values contain about 12, 8, 5, and 4% of dissolved Ni, Co, Zn, and Mn, respectively, in the form of hydrocarbonate complexes. The fraction of hydrocarbonate complexes is 50% lower in the waters of Bathonian–Callovian deposits, since the waters are ultrafresh. Carbonate complexes are not characteristic for other types of waters. The fraction of sulfate complexes of the elements is within 3–10%. No other complexes are characteristic for Mn and Co. Up to 8% of Ni and Zn are associated with dissolved organic matter.

The results of thermodynamic calculations for the distribution of dissolved occurrence forms of trace elements in spring waters of Balashikha urban district, % of total content of dissolved forms: ( 1 ), free ions; ( 2 ), carbonate complexes; ( 3 ), sulfate complexes; ( 4 ), chloride complexes; ( 5 ), nitrate complexes; ( 6 ), complexes of organic acids; ( 7 ), hydroxo complexes.

Cadmium was the only treated element for which the calculation resulted in significant amounts of chloride complex under an increase of chloride ion in the water: 11, 15, and 25% in the waters of the Volga, Upper-Gzhel, and Kalinin layer, respectively. The formation of chloride complexes is not characteristic for other elements, even in chloride waters (Below 1%).

The distributions of Cu and Pb by the occurrence forms in water are similar to each other and very different from that of other elements. The sulfate–hydrocarbonate waters of pH 6.6–6.9 (the waters of the Don–Moscow and Upper-Gzhel layers; the springs 4, 7, 7a, 9, and 9a) contain Cu and Pb commonly as hydrocarbonate complexes (48 and 42%), free ions (30 and 24%), and organic complexes (18 and 28%, respectively).

The fraction of Cu and Pb free ions increases to 47 and 39%, respectively, owing to the decrease of the fraction of complex compounds in ultrafresh waters of sporadic occurrence in the Bathonian–Callovian deposits. The decrease of pH values to 5.5–6.3 and a composition change in sulfate–chloride (the Volga water-bearing layer andsprings 1, 1a, and 2) and then mainly to chloride (the Kalinin alluvial layer, the springs 5 and 5a) results in the decrease of the fraction of carbonate complexes to 2–6 and 4–8%, while that of organic complexes increases to 48–60 and 60–70% and more (for Cu and Pb, respectively. The further decrease of pH to 5.3 and the composition change into nitrate–sulfate (the Mikulino–Kalinin lacustrine–marshy water-bearing layer, spring 6) causes the complete disappearance of carbonate complexes through an even greater increase of the fraction of complexes associated to organic matter. The role of sulfate complexes is subordinate everywhere (4% or less for Cu and 6% for Pb).

The distribution of dissolved occurrence forms of trace elements in spring waters of Balashikha urban district obtained by thermodynamic calculations agrees in general with the published data of surface freshwater basins that are undergoing no significant anthropogenic load (Gromova et al., 2016; Lipatnikova et al., 2016; Lipatnikova and Lubkova, 2021).

CONCLUSIONS

The springs of Balashikha urban district are characterized by fresh waters of 130–160 mg/L mineralization (430 mg/L on average) and pH values from subacidic to near neutral (pH 5.3–6.9).

Distinctions in the major component composition of spring waters that depend on a drained water-bearing layer were found. Thus, chloride calcic–sodium waters are characteristic for the Kalinin alluvial water-bearing layer. The locally slightly water-bearing Mikulino–Kalinin lacustrine–marshy layer produces nitrate–sulfate magnesium–calcic waters. The sulfate–hydrocarbonate calcic waters are characteristic for the Don–Moscow aquatic–glacial layer. The Volga layer is characterized by chloride–sulfate calcic (up to sodium–calcic and magnesium–calcic) waters. The waters of sporadic occurrence in the Bathonian-Callovian deposits are sulfate–hydrocarbonate calcic and are characterized by a high iron content. Sulfate–hydrocarbonate calcic waters are characteristic of the Upper-Gzhel water–bearing layer.

The spring waters are mainly characterized by an increased content of nitrate ion (up to 44 mg/L) although it does not exceed the TLV for potable waters. Moreover, a heightened content of ammonium ion (1.6–4.7 mg/L) was found in the waters of the Kalinin alluvial and Volga water-bearing layers.

The concentrations of trace elements are as a rule characteristic for the groundwaters of a leaching zone and, with rare exception, are below the TLVs of chemicals in the waters for the aquatic sources of potable, domestic, and economic uses. Heightened contents were found in waters of individual springs for manganese and iron standardized by organoleptic parameters of harmfulness. In this case, the registered values were below the sanitary standards prescribed by the WHO based on the upper level of a trace element supply for consumption.

The thermodynamic calculations of dissolved occurrence forms of trace elements showed that the prevailing forms for Sr, Ba, Fe, Mn, Zn, Ni, Co, and Cd are free ions, whereas Cu and Pb are characterized by carbonate and organic complexes.

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The study was supported by the “Development of integrated techniques of physical, forecast–prospecting, and environmental geochemistry” State budget theme (Contract no. 5-3-2021).

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Lipatnikova, O.A., Lubkova, T.N., Yablonskaya, D.A. et al. The Composition and Element’s Speciation in the Spring Waters of the Southern Part of the Balashikha Urban District (Moscow Region). Moscow Univ. Geol. Bull. 78 , 423–436 (2023). https://doi.org/10.3103/S0145875223030110

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Received : 31 October 2022

Revised : 02 November 2022

Accepted : 22 May 2023

Published : 07 October 2023

Issue Date : June 2023

DOI : https://doi.org/10.3103/S0145875223030110

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