On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan

Djamshed A. Abdushukurov; Daler Abdusamadzoda; Octavian G. Duliu; Inga Zinicovscaia; Pavel S. Nekhoroshkov

doi:10.3390/app12062763

On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan

Abdushukurov, Djamshed A.;Abdusamadzoda, Daler;Duliu, Octavian G.;Zinicovscaia, Inga;Nekhoroshkov, Pavel S. 2022-03-08 00:00:00 applied sciences Article On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan 1 1 , 2 2 , 3 , 4 , 2 , 5 Djamshed A. Abdushukurov , Daler Abdusamadzoda , Octavian G. Duliu * , Inga Zinicovscaia and Pavel S. Nekhoroshkov Institute of Water Problems, Hydropower and Ecology of Academy of Science, 14a Ainy Str., Dushanbe 734042, Tajikistan; abdush_dj@mail.ru (D.A.A.); martinez-91@mail.ru (D.A.) Joint Institute for Nuclear Research, 6, Joliot Curie Str., 141980 Dubna, Russia; zinikovskaia@mail.ru (I.Z.); p.nekhoroshkov@gmail.com (P.S.N.) Department of Structure of Matter, Faculty of Physics, University of Bucharest, Earth and Atmospheric Physics and Astrophysics, 405, Atomistilor Str., 077125 Magurele, Romania Geological Institute of Romania, 1, Caransebes Str., 012271 Bucharest, Romania Department of Nuclear Physics, Horia Hulubei National Institute for R&D in Physics and Nuclear Engineering, 30 Reactorului Str., P.O. Box MG-6, 077125 Magurele, Romania * Correspondence: o.duliu@upcmail.ro Abstract: To assess the geochemical features of sedimentary material of Zarafshon river, (Western Tajikistan) catchment basin, the mass fractions of 38 major and trace elements were determined by Instrumental Neutron Activation Analysis (INAA) in 2 116 paired samples of sediments and soils collected along the Zarafshon River and its main tributaries from the sources to Tajik—Uzbek border. At each collecting location, the distance between sediments and soils’ sampling was no greater Citation: Abdushukurov, D.A.; than 10 m allowing the studying of the interrelation between sediments and soils. This evidenced Abdusamadzoda, D.; Duliu, O.G.; a signiﬁcant similarity between paired soils and sediments’ samples, including the potentially Zinicovscaia, I.; Nekhoroshkov, P.S. contaminating elements As, Sb and Hg, whose mass fractions in some places were signiﬁcantly On the Geochemistry of Major and Trace Elements Distribution in higher than for the Upper Continental Crust (UCC) and North American Shale Composite (NASC), Sediments and Soils of Zarafshon suggesting a common provenience. At the same time, the distribution of major, as well as of River Valley, Western Tajikistan. Appl. incompatible trace elements, Sc, Zr, REE, Th, and U, in spite of geological diversity of the Zarafshon Sci. 2022, 12, 2763. https://doi.org/ river catchment basin, suggest a possible felsic origin of investigated material. 10.3390/app12062763 Keywords: Zarafshon; Tajikistan; sediments; soils; INAA; felsic material; REE Academic Editors: Claudia Stihi and Antoaneta Ene Received: 7 February 2022 Accepted: 3 March 2022 1. Introduction Published: 8 March 2022 The Zarafshon River originates at the Zarafshon glacier, at an altitude of 2775 m, Publisher’s Note: MDPI stays neutral at the junction of the Turkestan and Zarafshon ranges, both of them belonging to the with regard to jurisdictional claims in western sector of the Pamir-Alay system [1]. The initial part of the river, about 300 km long, published maps and institutional afﬁl- lies in a narrow, deep valley. On the southern left bank, ﬂowing between the Turkestan iations. and Zarafshon ranges, it receives the Yagnob, Arthuch and Mogiyon rivers, as well as many small tributaries (Figure 1) [1–3]. After the city of Panjakent, the river follows a ﬂat region, crosses the Tajikistan-Uzbekistan border, passes Samarkand and Bukhara, to ﬁnally disappear in the desert in the vicinity of the city of Karakul, without reaching the Copyright: © 2022 by the authors. Amu Darya River [3,4]. Its catchment basin, with an area of 17,700 km , covers diverse Licensee MDPI, Basel, Switzerland. geological formations spread from the alpine zone, 3200–3500 m above sea level, to less This article is an open access article than 150 m elevation westward towards the city of Karakul. In the Zarafshon mountain distributed under the terms and gorges, below 1500 m there are small areas of semi-savannahs as well as mountain forests. conditions of the Creative Commons Attribution (CC BY) license (https:// Here, regosols are prevalent [5], while in the western sector of Zarafshon Valley luvisols creativecommons.org/licenses/by/ formed on loess deposits are common. Moreover, in mountain gorges, terraces of alluvial 4.0/). Appl. Sci. 2022, 12, 2763. https://doi.org/10.3390/app12062763 https://www.mdpi.com/journal/applsci Appl. Sci. 2022, 12, 2763 2 of 21 Appl. Sci. 2022, 12, x FOR PEER REVIEW 3 of 22 deposits and outﬂow cones of lateral tributaries serve as the basis for soil components (Figure 1a, Table A1). Figure 1. Figure 1. The Themap of Zarafshon Valley ( map of Zarafshon Valley (a a)); ; s showing howing its po its position sition with within in Taj Tajikistan ikistan territory ( territory (b b). ). Appl. Sci. 2022, 12, 2763 3 of 21 The “Zarafshon” name, which in Farsi means “spreader of gold”, reﬂects the existence of ore ﬁelds along the river valley which, together with other outcrops of nonferrous ores makes it a mineral rich province requiring a detailed investigation. Although the total population of Zarafshon valley does not exceed 400,000 inhabitants, mainly populating small villages, the existence of non-ferrous ore outcrops could represent the main source of down-stream contamination, previously analyzed in [6]. For this reason, the distribution of major and rock-forming elements as well as of incompatible lithophile elements such as Sc, Ti, V, Cr, Zr, lanthanides (LN) Th or more soluble U together with siderophile Co and Ni were chosen for this study. All of them play a signiﬁcant role in geochemistry and pedology as tracers of the origin of natural material which, disintegrated during weathering and erosion, represents the main con- stituents of sediments and soils [7–10]. Besides them, there are other trace elements such as V, Cr, Co, Ni, Zn, As, Sb, or Hg, intensively used in diverse industrial processes, and, the presence of which, at levels signiﬁcantly exceeding the natural ones, are related to an anthropogenic contamination which could be industrial [11,12] or due to urban as well as rural agglomerations [13]. According to [14], soil is a result of the combined action of weather, geographic relief, organisms and human activity on the parent mineral sub- strate, all of them continuously interacting. The actual soil is no older than Pleistocene, i.e., 2.59 Ma almost coincident with the onset of Northern hemisphere glaciation. In turn, sediments represent a fragmented mineral substrate under the action of weathering and erosion and which is transported at long distances by the action of water, wind or ice and ﬁnally deposited. With respect to soil, sediments consist of unconsolidated clastic material with a reduced amount of organic matter. When consolidated by natural cementation processes, sediments turn into sedimentary rocks such as siltstone, sandstone, shale, etc. Both sediments and soils preserve the ﬁngerprint of the parental mineral substrate, which, under the action of external factors, evolve in a different manner. Collected from the same places and investigated in tandem, these sedimentary materials could bring a bonus of information concerning the local geochemistry as well as their interrelationship. In this regard, in the period of spring-autumn, between 2015 and 2018, the Institute of Water Problems, Hydropower and Ecology of the Academy of Science of Tajikistan organized a ﬁeld expedition to collect the most representative samples of sediments and soils from the Tajik sector of Zarafshon catching basin. For a better characterization of the soil–sediments interrelation, we collected from the same places distributed along the Zarafshon River and its main tributaries, including both sediments and soils samples (Figure 1a). In the case of presumed contaminated locations, mainly nonferrous mines and processing plants, samples were collected upstream and downstream at distances of no more than 10 to 20 m from them. This permitted the collecting of 116 sediments, as well as an equal number of soils samples to be analyzed at the Neutron Activation Analysis Section of the Frank Laboratory of Neutron Physics (FLNP) of the Joint Institute for Nuclear Research (JINR), Dubna, Russian Federation. For a better precision and accuracy, we have used the Instrumental Neutron Activation Analysis (INAA), in both its thermal and epithermal variants [15,16]. It is worth mentioning that INAA was chosen due its capacity to determine the mass fractions of up to 40 elements, 38 in the case of this study, without any preliminary processing prone to induce systematic errors (Table 1) [16]. Appl. Sci. 2022, 12, 2763 4 of 21 Table 1. The mass fraction of investigated elements in sediments and soils as well as the main literature references: UCC [17]; North American Shale Composite NASC [18]; Post Archaean Aus- tralian Shale (PAAS) [8]; Suspended Matter of the World’s Rivers (SMWR) [19]; as well as Average World Suspended Sediments (AWSS) [20]. Oxides’ mass fraction expressed in wt.%, in mg/kg for other elements, excepting Hg of which the mass fraction is expressed in g/kg. CSU represents the Combined Standard Uncertainty [21]. Element Sediment CSU Soils CSU UCC NASC PAAS SMWR AWSS SiO 62.75 12.65 59.39 9.7 66.62 64.48 62.8 54.76 54.34 TiO 0.62 0.22 0.83 1.06 0.64 0.72 1 0.65 0.73 Al O 9.9 3.52 12.92 4.07 15.4 16.9 2.2 16.31 16.48 2 3 FeO 3.79 2.5 5.78 2.01 5.04 5.7 18.9 6.47 7.47 MnO 0.07 0.07 0.09 0.03 0.1 0.06 0.11 0.15 0.22 MgO 6.32 3.42 5.8 2.72 2.48 2.85 — 2.39 2.09 CaO 10.59 10.71 9.46 9.06 3.59 3.56 1.3 3.64 3.62 K O 2.4 0.99 2.83 0.79 2.8 3.99 3.7 2.59 2.04 Na O 1.4 0.79 0.9 0.41 3.27 1.15 1.2 1.11 0.96 Sc 9.6 4 11 5 14 15 16 14 18 V 101 56 254 1500 97 — — 120 129 Cr 71 40 90 57 92 124 110 85 130 Co 11.5 6.4 14.5 7.1 17.3 — — 19 22.5 Ni 46 32 65 31 47 58 55 50 74 Zn 102 57 119 54 67 — —- 130 208 As 63 254 84 600 4.8 28.4 — 14 36.3 Br 2.6 4.3 1.9 1.6 1.6 0.9 — 9 21.5 Rb 92 41 103 39 84 126 160 77.0 79 Sr 143 63 177 100 320 142 200 150.0 187 Zr 220 133 210 101 193 200 210 150.0 160 Sb 59 560 38 270 0.4 — — 1.4 2.2 Cs 4.5 570 7.5 3.6 4.9 5.2 15 5.2 6.3 Ba 724 450 784 500 624 636 650 500 522 La 28 14 32 12 31 31 38.2 32 37 Ce 53 26 61 25 63 67 79.6 68 73.6 Nd 27 15 32 17 27 27 33.9 29 32.2 Sm 5 2.5 6.3 3.4 4.7 5.6 5.6 5.8 6.1 Eu 0.9 0.6 1.1 0.8 1 1.2 1.1 1.4 1.3 Gd 3.9 3.3 2.9 2.4 4 — 4.7 5.6 5.3 Tb 0.7 0.3 1 0.4 0.7 0.9 0.8 0.8 0.8 Tm 0.3 0.3 0.5 0.5 0.3 — 0.4 0.4 0.4 Yb 1.9 1.2 2.2 1.5 2 3.1 2.8 2.5 2.1 Hf 5.5 3 5.8 2.6 5.3 6.3 — 4.4 4 Ta 0.8 0.4 1 0.5 0.9 1.12 14.6 0.9 1.3 W 2.5 5.7 2.8 2.7 1.9 2.1 — 1.4 2 Hg 2.5 14.7 1.1 4.5 0.1 — — 0.1 — Th 8.9 4.3 10.9 3.5 10.5 12.3 3.2 10 12.1 U 3 1.5 3.9 1.7 2.7 2.7 — 2.4 3.3 2. Hypothesis and Research Objectives As presented before, the Zarafshon catchment basin covers a diversity of geological formations of which the origin dates back to Oligocene. This was when, as mentioned in [22], a Jurassic basin ﬁlled with continental sediments, under the pressure exerted by the Hindustan continental plate, and generated the Pamir-Alay system. Therefore, it is to be expected that the materials of which the Zarafshon valley is made up to contain a signiﬁcant proportion of crustal matter. In time, due to weathering, this tends to be transported by the river and its tributaries as suspended load and deposited on river beds and river banks, as the mineral constituents of soils. Accordingly, the main goals of this study consist of: (i) to verify to what extent the geochemistry of depositional material, i.e., sedi- ments and soils, can be related to crustal material, better approximated by UCC [17] Appl. Sci. 2022, 12, 2763 5 of 21 and NASC [18], PAAS [8] in the case of soils, and SMWR [19], as well as AWSS [20] for sediments; (ii) to evidence any interrelationship between the geochemistry of sediments and adjacent soils, as it is reﬂected by the distribution of major rock forming, as well as incompatible elements. It should be noted that we have paid special attention to those elements whose presence is not related to any industrial activities such as mining, as the presence and distribution of the Presumably Contaminating Elements (PCE) on the Zarafshon catchment basin were previously analyzed in [6]. The results of our study performed under these circumstances will be further presented and discussed. 3. Geological Setting Due to its location between two important mountain ranges—Turkestan and Zarafshon– the Zarafshon catchment’s basin covers a variety of lithologies of which clastic material represents the main component of sediments and bordering soils. According to [22], the actual Turkestan and Zarafshon ranges evolved during Oligocene from a Jurassic basin ﬁlled with continental, shallow-water marine and lagoonal sediments of which crustal origin seems to inﬂuence its present geochemistry. This was the main rea- son for which we have chosen UCC [17] and NASC [18] as the most appropriate descriptor of investigated material. At present, Djidjikrut, Fondarya, both tributaries of the Yagnob, as well as Mogiyon and its tributaries have the most important contribution to the mineral composition of Zarafshon sedimentary material [23,24]. The Djidjikrut River ﬂowing in the Ayni district passes through clays, marls, lime- stones, dolomites and salts, signiﬁcantly inﬂuencing the mineral composition of water and neighboring sediments and soils. At the conﬂuence with the Zarafshon (Yagnob river), is located the Djidjikrut ore ﬁeld related to Zarafshon-Gissar mercury-antimony belt, and dating to Middle and Upper Paleozoic. Antimonite, cinnabar and metacinnabarite are the main minerals of the Djidjikrut ore ﬁeld, while pyrite and marcasite with an admixture of Co, Ni, Cu, As, Sb, Au, Te and Bi, realgar and orpiment, as well as hematite and sphalerite are common minerals too. For this reason, at the conﬂuence of the Djidjikrut and Yagnob rivers, on the northern slope of the Gissar range, the Anzob mining and processing plant is operating [5] with the ﬁnal release of Hg-Sb concentrate, an important source of downstream contamination (Figure A1). The Yagnob River ﬂows westward through the narrow mountain gorge along the southern edge of the Zarafshon mountains, being the ﬁrst tributary of the Fondarya River. The total length of the Yagnob river is 114 km with a basin area of 1660 km , while the mineral composition of sediments and soils of its upper reaches is still poorly investigated. Downstream, near the conﬂuence with Fondarya, the Fon-Yagnob coal deposit occupies almost the entire left-bank site between the Djidjikrut and Pasrud tributaries [25]. Here, due to exothermic oxidation of the sub-surface coal layers, rich in pyrite and marcasite, a self-ignition process contaminated neighboring locations. Here, the paralava, a product of complete melting and (partial) recrystallization of local rocks generated by the high temperature attained during underground coal combustion, consists of almost melted sediments enclosing coal seams [26–28]. It is supposed that the underground coal ﬁre may contribute to diagenesis of some REE minerals such as godovikovite, efremovite, maskanite, and so on [27–30]. The Fondarya River with a signiﬁcant catchment basin of 3230 km is formed by the conﬂuence of the Yagnob and Iskandardarya, which then crosses the Zarafshon ridge and ﬂows into the Zarafshon river. In addition, the Fondarya is fed by the waters of the Sarvoda river which originates from the Alovdin lakes, as well as the lower and upper Kumarg tributaries, Chore and Pete (Figure 1a). Appl. Sci. 2022, 12, 2763 6 of 21 It should be noted that in the upper ﬂows of the Iskandardarya river operates the mining and processing plant “Tolko-Gold”, which extracts and processes Au, Ag, Hg, and Sb ore as well as ﬂuorite. The mining operation is also carried out at the gold deposit in the Kumargi Bolo gorge. The Chore River gorge is classiﬁed as gold-quartz deposits at the Turkestan-Chore zones of Central Tajikistan [31]. This deposit was discovered in 1960 and intensively exploited during 1974–1984 mainly for pyrite and arsenopyrite which represented more than 95% of all ore minerals together with small amounts of antimonites, chalcopyrite, sphalerite, pyrrhotite, and others [32]. The Pete tributary ﬂows between the Pete-Takfon ore ﬁeld hosting Takfon, Pete, Simich, and other deposits. In the geological structure of this ore ﬁeld, Paleozoic formations are widely developed, which are represented by Silurian (shales, limestones, dolomites with interlayers of quartzites), Devonian (siliceous and micaceous shales with interlayers of cherts and limestones), Carboniferous (limestones with horizons of clay shales, sandstones) and Cong deposits. To the south of the ore ﬁeld area, the complex of Paleozoic formations is overlapped by sub-platform sediments of the Mesozoic. The Igneous formations are represented by the Pete intrusions of granodiorites, dikes of granodiorite-porphyry, and lamprophyres. There are also tin and silver, lead, and zinc-containing ores [33]. 2, The Mogiyon river (Figure 1a), with a length of 68 km and a basin area of 1100 km is one of the largest Zarafshon tributaries. From the source to the village of Mogiyon in a narrow valley, the river ﬂows in a northern direction, cutting through the Zarafshon ridge with a deep transverse gorge. Further on, having received its largest tributary–the Shing River–it continues to ﬂow in a narrow rapids channel with a width of up to 10 m. Nine kilometers above the city of Panjakent, leaving the gorge and passing through the village of Sujina, it then falls into the Zarafshon River (Figure 1). Between the Shing and Mogiyon interﬂuve is located the Taror ore ﬁeld, which belongs to the Western Zarafshon- Gissar metallogenic zone [34]. However, along with gold-sulﬁde mineralization, silver-tin-base metal mineralization, localized in its upper and middle horizons, is also developed. The silver deposits in the Taror ore ﬁeld belong to the Mirkhant deposit and its mineralization is predominantly rep- resented by a silver-tin-polymetallic association spatially combined with sulﬁde, showing the closest correlation between Ag and Sb [27]. It is worth noting that in the Tarror gold ore deposit operates the Joint Venture “Zarafshon” whose main product consists of Ag-Au alloy [35]. In addition, along Zarafshon river and some of its main tributaries there is an active mining and metallurgical industry, based on the extraction and processing of non-ferrous metals. Among them, the Anzob mining and processing plant (AMPP), Taror gold ore plant (TGOP), Upper Kumarg and Kanchoch AGOK and TGOP specialized in the production of antimony-mercury concentrates and, respectively, gold. All of them could be regarded as a potential source of anthropogenic contamination which needs continuous monitoring extended to both the sediments and neighboring soils [35]. In this regard, the investigated Zarafshon valley together with some of its tributaries are the object of controversy between scientists and environmental experts representing governmental and non-governmental organizations. For this reason, it is not entirely correct to assess the environmental state of a particular region without paying a special attention to its geochemical features. 4. Materials and Methods 4.1. Sampling An equal number of 116 sediments and 116 soils samples were collected in the in- vestigated area (Figure 1a), using an AMS 12 Multi Stage sediments Sampler (AFMS Inc., American Falls, ID, USA) equipped with tubular glass sampler. Unconsolidated columns of sediment, 20 to 30 cm long, were handpicked from the riverbeds during a high-water period. As at altitudes greater than 2000 m, the soil cover is less developed, so that soil Appl. Sci. 2022, 12, 2763 7 of 21 columns were no longer than 10 cm. For our study we retained the top soil (horizon A), as we were also interested to evidence recent contamination processes [6]. We collected soil samples always nearby the river banks. After collecting, any traces of vegetable matter such as fragments of grass and grass roots, leaves, wood pieces, as well as fragments of rock were carefully removed. From each sampling point, three sub-samples of collected material, e.g., sediment or soil, covering an area of about 10 m were gathered and carefully mixed to form a composite sample. Any possible cross-contamination was avoided by washing the glass sampler before any sampling with a solution of diluted hydrochloric acid with deionized water and soaking them with disposable cotton serves. To evidence any correlation between sediments’ and soils’ geochemistry, sediment and soil samples were collected in the same places, with two exceptions, and the dis- tance between the sediments and the soils’ sampling location never exceeded 5–10 m (Table 1) and [36]. The same distances separated mines, adits or tunnels of the downstream collecting places. 4.2. Samples Preparation Samples consisting of silty grayish sand without organic detritus were placed into the plastic container with cooled refrigerant and kept at 4 C. In the laboratory, all samples were dried at 70 C at constant weight and ground. Finally, the dried material was sieved using a 0.425 mm (42 mesh) sieve, homogenized and sent to the Frank Laboratory of Neutron Physics (FLNP) of the Joint Institute for Nuclear Research (JINR) for further INAA. Here, 10 g of each sample were homogenized again for 15 min in a planetary ball mill (PULVERISETTE 6, Fritsch Laboratory Instruments GmbH, Idar-Oberstein, Germany) at 400 rpm. To increase the precision and accuracy of measurements, six aliquots of about 0.3 g were selected from each sample and independently analyzed. 4.3. INAA Measurements and Quality Control Before irradiation at the IBR-2 reactor of the JINR FLNP in Dubna, each aliquot was packed in polyethylene bags for the determination of short-living isotopes (three aliquots) and in aluminum foil (three aliquots) for long-living ones. It is worth mentioning that the mass fractions of short-living isotopes were determined by thermal neutron activation while in the case of long-living isotopes we have used epithermal neutrons. More details concerning irradiation time and neutron ﬂux densities in each irradiation channel can be found in [37]. After irradiation, the gamma spectrum of each sample was recorded using a HPGe detector with a resolution of 1.9 keV for the Co 1332 keV line, analyzed by means of a Genie 2000 Canberra software and processed by a proprietary software [37]. This permitted determination of the mass fraction of each of the 38 considered elements together with the associated CSU [21]. In all cases, the CSU was estimated by taking into account the statistical error, inﬂuence of measurement geometry, detector efﬁciency, the content, as well as the error of each element for all Certiﬁed Standard Material (CSM) utilized for calibration. To avoid any environmental contamination, all resulting radioactive materials were deposited in a permanent low activity repository. The quality control was assured in the case of sediments and soils by a simultane- ous analysis of Standard Reference Materials (SRM) provided by the National Institute for Standard and Technologies (NIST), i.e., 1633c Coal ﬂy ash, 667 Estuarine sediment, 2710 Montana Soil and 1547 Peach leaves for short half-life time isotopes. In the case of long life-time isotopes, the best results were obtained using–2709 Trace elements in soil, 1632c–Trace elements in coal, 690CC–Calcareous soil, 2709a–San Joaquin soil, 1632c–Trace elements in coal and SRM-AGV2–Andesite. Further, by using all of the above-mentioned SRM a Group of Standard Sample (GSS) [37,38] was realized which permitted the choice of the most appropriate SRM lines to minimize errors in determining the mass fractions of all investigated elements. It is worth Appl. Sci. 2022, 12, 2763 8 of 21 mentioning that GSS is a proprietary software which, besides helping to determine the mass fractions of chosen elements, it allowed the calculation of the extent to which the mass fractions of SRM corresponded to certiﬁed ones [37,38]. Following this procedure, the accuracy quantiﬁed by means of standard deviation corresponding to each group of three aliquots was lower than 10%. In the case of SRM, the CSU varied between 3 and 15%, higher in the case of REE, but never greater than 20%. It is worth mentioning that for all 38 investigated elements, the detection limit was of 1 mg/kg and lower [37,38]. To illustrate the sensitivity and accuracy of INAA measurements following the CSS software, in Table A2 we have reproduced, as an example, the experimentally determined mass fractions of SRM 2709. Similar determinations were completed in the case of all utilized SRM. 5. Results and Discussion A complete set of data concerning the mass fractions of all 38 elements in the investi- gated samples are provided in the Mendeley repository [36], while Table 1 reproduces only the mass fractions’ average values together with corresponding values of the UCC [17], NASC [18], PAAS [8], SMWR [19], as well as AWSS [20]. In interpreting compositional data of river sediments and adjacent soils, the geochem- istry of local formations usually plays a determinant role. Additionally, due to a variable mobility, different mineral fractions are mixed and deposited along river beds depending on water speed, grain sizes and speciﬁc gravity. In this regard, Figure 2 illustrates the mass fractions of investigated elements in sediments normalized to UCC (Figure 2) [16], and in soils normalized to SMWR (Figure 2) [19]. The UCC [17] was chosen as an appropriate descriptor of the continental crust, while SMWR [19] drew on the lithogenesis theory [39], according to which, the mobilization of suspended and dissolved materials in drainage basins represent the initial stage of pedogenesis. Here, a signiﬁcant fraction of chemical elements including highly mobile alkaline and calc-alkaline ones were transported as suspended sediments and deposited along river beds and banks. Therefore, other descriptors such as NASC [17], AWSS [19] or PAAS [8] showed to be almost identical. According to Table 1 and [36], the elemental composition of sediments and soils appears, excepting chalcophile Zn, As, Sb ad Hg, closer to UCC [17] and SMWR [19]. After a careful analysis of the experimental data presented in [36], mass fractions of potentially contaminating elements As, Sb and Hg showed increased values only for samples collected in the vicinity of mines and adits located on the Djidjikrut, Kanchoch, Chore and Mogiyon tributaries (Figures 1a, 2 and A1). This ﬁnding is well evidenced in Figure 3a, where the As, Sb and Hg standard devi- ations appear disproportionately high due to the fact that in a very few places, such as mines or mine adits, their mass fractions exceeded the UCC [17] one by two to three orders of magnitude. Excepting these, the average mass fractions of investigated elements were shown to be relatively closer in both sediments and soils, as suggested by ANOVA analysis (Table 2) and by both biplots reproduced in Figure 3. In addition, a Spearman’s correlation coefﬁcient of 0.83 sustains this observation (Figure 3b). Appl. Sci. 2022, 12, x FOR PEER REVIEW 10 of 22 Appl. Sci. 2022, 12, 2763 9 of 21 Figure 2. Box-plots illustrating the distribution of investigated elements in Zarafshon sediments Figure 2. Box-plots illustrating the distribution of investigated elements in Zarafshon sediments (lower); and soils (upper). All mass fractions of soils normalized to UCC [17] and sediments to (lower); and soils (upper). All mass fractions of soils normalized to UCC [17] and sediments to SMWR [19]. The values corresponding to As and Hg are divided by 10 and by 100 in the case of Sb. SMWR [19]. The values corresponding to As and Hg are divided by 10 and by 100 in the case of Sb. Appl. Sci. 2022, 12, x FOR PEER REVIEW 11 of 22 This finding is well evidenced in Figure 3a, where the As, Sb and Hg standard deviations appear disproportionately high due to the fact that in a very few places, such as mines or mine adits, their mass fractions exceeded the UCC [17] one by two to three orders of magnitude. Excepting these, the average mass fractions of investigated elements were shown to be relatively closer in both sediments and soils, as suggested by ANOVA Appl. Sci. 2022, 12, 2763 10 of 21 analysis (Table 2) and by both biplots reproduced in Figure 3. In addition, a Spearman’s correlation coefficient of 0.83 sustains this observation (Figure 3b). Figure 3. The sediment to soil ratio of mass fractions of investigated elements (red line) as well as Figure 3. The sediment to soil ratio of mass fractions of investigated elements (red line) as well as the corresponding standard deviation (gray background) (a); and a biplot illustrating the reciprocal the corresponding standard deviation (gray background) (a); and a biplot illustrating the reciprocal distribution of investigated elements in sediments and soils excepting the Zn, As, Sb and Hg, i.e., distribution of investigated elements in sediments and soils excepting the Zn, As, Sb and Hg, i.e., elements whose mass fractions in some places exceeds the UCC [17] ones by two to three orders of elements whose mass fractions in some places exceeds the UCC [17] ones by two to three orders of magnitude (b) (Table 1) [36]. Spearman’s correlation coefficient of 0.837 at p < 0.01. magnitude (b) (Table 1) [36]. Spearman’s correlation coefﬁcient of 0.837 at p < 0.01. Table 2. The results of two-sample ANOVA tests illustrating the probability the major and trace Table 2. The results of two-sample ANOVA tests illustrating the probability the major and trace elements being closer in soils and sediments. The results are based on the average mass fractions elements being closer in soils and sediments. The results are based on the average mass fractions values reproduced in Table 1. values reproduced in Table 1. ANOVA Two-Sample Test T-Test F-Test Mann–Whitney Anderson–Darling ANOVA Two-Sample Test Elements Equal Mean Equal Variance Equal Median Equal Distribution T -Test F-Test Mann–Whitney Anderson–Darling Elements Equal Mean Equal Variance Equal Median Equal Distribution Major elements 0.99 0.87 1.00 1.00 Trace elements 0.77 0.59 0.73 0.97 Major elements 0.99 0.87 1.00 1.00 Trace elements 0.77 0.59 0.73 0.97 Major elements: SiO2, TiO2, Al2O3, FeO, MnO2, MgO, CaO, K2O, Na2O Trace elements: Sc, V, Cr, Co, Ni, Zn, As, Br, Rb, Sr, Zr, Sb, Cs, Ba, La, Ce, Nd, Sm, Eu, Gd, Tb, Tm, Yb, Hf, Ta, W, Hg, Th, U Major elements: SiO TiO Al O FeO, MnO MgO, CaO, K O, Na O 2, 2, 2 3, 2, 2 2 Trace elements: Sc, V, Cr, Co, Ni, Zn, As, Br, Rb, Sr, Zr, Sb, Cs, Ba, La, Ce, Nd, Sm, Eu, Gd, Tb, Tm, Yb, Hf, Ta, W, Hg, Th, U Figure 3a evidenced also that the ratio between the same elements in sediments and soil slightly varies around one, excepting the above mentioned PCE As, Sb and Hg and, Figure 3a evidenced also that the ratio between the same elements in sediments and soil to a slightly lesser ex varies tent, Na o around f whone, ich the excepting average ma the s above s fraction was mentioned sligh PCE tly highe As, Sb r in and seHg diments and, to than a lesser in soiextent, ls, as wNa ill be of di which scusse the d in average the next s mass ection. fraction was slightly higher in sediments than in soils, as will be discussed in the next section. 5.1. Major Elements 5.1. Major Elements The average values of the mass fractions of major, rock-forming elements excepting The average values of the mass fractions of major, rock-forming elements excepting for MgO and CaO showed to be relatively closer to UCC [17], NASC, [18], PAAS [8], or for MgO and CaO showed to be relatively closer to UCC [17], NASC, [18], PAAS [8], or other sedimentary systems such as SMWR [19], or Average World Suspended Sediments other sedimentary systems such as SMWR [19], or Average World Suspended Sediments AWSS [20] (Table 1). AWSS [20] (Table 1). Silica represents the major constituent of all investigated samples, its mass fraction Silica represents the major constituent of all investigated samples, its mass fraction of 34.64 wt.% to 84 wt.% (62.8 ± 11.9 wt.% average) for sediments and of 31.53 wt.% to of 34.64 wt.% to 84 wt.% (62.8 11.9 wt.% average) for sediments and of 31.53 wt.% to 75.12 wt.% (59.4 8.8 wt.% average) for soils. On discriminating diagrams Na O + K O vs. 2 2 SiO (Figure 4a), SiO -Al O -Na O + K O + CaO (Figure 4b) and K O-Al O -Na O + CaO 2 2 2 3 2 2 2 2 3 2 (Figure 4c) the composition of investigated materials points towards a somewhat felsic to intermediate origin with a small contribution of maﬁc material as was the case in the Pete intrusion [5,24] (Table 1). Its average mass fraction was closer to the UCC [17] but with only a few exceptions in the sediments collected in the vicinity of the Anzob tunnel, Sarvoda 1, and Sarvoda 2 as well as soils from Chore 1 and 3, Djidjikrut 1, Obi Sara 1, Saritag 2, as well Appl. Sci. 2022, 12, x FOR PEER REVIEW 12 of 22 75.12 wt.% (59.4 ± 8.8 wt.% average) for soils. On discriminating diagrams Na2O + K2O vs SiO2 (Figure 4a), SiO2-Al2O3-Na2O + K2O + CaO (Figure 4b) and K2O-Al2O3-Na2O + CaO (Figure 4c) the composition of investigated materials points towards a somewhat felsic to intermediate origin with a small contribution of mafic material as was the case in the Pete Appl. Sci. 2022, 12, 2763 11 of 21 intrusion [5,24] (Table 1). Its average mass fraction was closer to the UCC [17] but with only a few exceptions in the sediments collected in the vicinity of the Anzob tunnel, Sarvoda 1, and Sarvoda 2 as well as soils from Chore 1 and 3, Djidjikrut 1, Obi Sara 1, Saritag 2, as well as Sarvoda 1 to Sarvoda 7 (Figures 1a and A1). In all locations, the lower as Sarvoda 1 to Sarvoda 7 (Figures 1a and A1). In all locations, the lower content of silica content of silica is due to an increased content of calcium oxide of which mass fractions is due to an increased content of calcium oxide of which mass fractions varied between varied between 26 and 47 wt.% (Table 1). 26 and 47 wt.% (Table 1). Figure Figure 4. 4. Discriminating Discriminating total total alkali alkali m metal etal ox oxides ides vs. vs.SiO SiO2biplot biplot( ( aa );)ternary ; ternary SiO SiO -Al 2-AlO 2O3 -Na -Na2O O + + K K 2O O 2 2 2 3 2 2 + CaO (b); and K-A-CN (c) diagrams illustrating the preponderance of felsic material in Zarafshon + CaO (b); and K-A-CN (c) diagrams illustrating the preponderance of felsic material in Zarafshon sediments and soils as well as a small fraction of weathered material. sediments and soils as well as a small fraction of weathered material. Aluminum Aluminum o oxide xide showe showed d in sed in sediments iments an an av average erage mass mass frac fraction tion 9.91 9.91 ± 3 3.2 .2 wt.%, wt.%, smaller than the soils’ one of 12.92 3.7 wt.%, both of them lower than the UCC [17] smaller than the soils’ one of 12.92 ± 3.7 wt.%, both of them lower than the UCC [17] and and NASC [17] (Table 1). At the same time, the sodium oxide has an average mass NASC [17] (Table 1). At the same time, the sodium oxide has an average mass fraction in fraction in sediments and especially in soils smaller than the corresponding UCC [17] sediments and especially in soils smaller than the corresponding UCC [17] (Table 1), (Table 1), suggesting a low content of plagioclase, and by consequence predominance of suggesting a low content of plagioclase, and by consequence predominance of a a sedimentary substrate (Figure 4a,b). This ﬁnding is illustrated by the discriminating sedimentary substrate (Figure 4a,b). This finding is illustrated by the discriminating diagram SiO -Al O -Na O + K O + CaO (Figure 4b) where some points are shifted towards 2 2 3 2 2 lower SiO content, which could be due to an increased content of CaO whose mass fraction in some places reached 28% [36]. It is worth remarking that CaO correlates positively only with MgO, in sediments as well as in soils (Table A3), suggesting the presence of dolomite CaMg(CO ) . Besides these, the K-A-CN ternary diagram suggests a weak inﬂuence of 3 2 weathering on both sediments and soils, expressed by a reduced fraction of total alkali–calc- alkali oxides Na O + CaO of which normalized values appear smaller than 0.25 (Figure 4c). 2 Appl. Sci. 2022, 12, x FOR PEER REVIEW 13 of 22 diagram SiO2-Al2O3-Na2O + K2O + CaO (Figure 4b) where some points are shifted towards lower SiO2 content, which could be due to an increased content of CaO whose mass fraction in some places reached 28% [36]. It is worth remarking that CaO correlates positively only with MgO, in sediments as well as in soils (Table A3), suggesting the presence of dolomite CaMg(CO₃)₂. Besides these, the K-A-CN ternary diagram suggests a weak influence of weathering on both sediments and soils, expressed by a reduced fraction of total alkali–calc-alkali oxides Na2O + CaO of which normalized values appear smaller than Appl. Sci. 2022, 12, 2763 12 of 21 0.25 (Figure 4c). The mass fractions of the other major elements oxides, i.e., TiO2, FeO, and MnO were closer to the UCC [17] values in conformity with the previous suppositions concerning a The mass fractions of the other major elements oxides, i.e., TiO , FeO, and MnO were rather felsic origin of investigated material (Table 1). closer to the UCC [17] values in conformity with the previous suppositions concerning a rather felsic origin of investigated material (Table 1). 5.2. Trace Elements 5.2. Trace Elements More data concerning the origin of investigated sedimentary materials can be inferr Mor ed ana e data lyzin concerning g the dist the ribu origin tion oof f tr investigated ace elements sedimentary and especially, materi as men als can tion bee inferr d in the ed analyzing Introducti the on, distribution of those cons ofitrace dered in elements compat and ible especially and insolub , as mentioned le such as in Sc, Zr, the Intr La oduction, , Ce, Nd, Sm, Eu, Gd, Tm, Yb, Th as well as U and, to a lower extent, Cr and Ni [6,7,40]. of those considered incompatible and insoluble such as Sc, Zr, La, Ce, Nd, Sm, Eu, Gd, Tm, Yb, Th Notably as well, th ase felsic rocks U and, to a lower are richer extent, in Th Cr and and ligh Ni [6t ,7 RE ,40 E, where ]. as mafic rocks contain more Notably Sc, Cr,, the Co, N felsic i an rocks d an i arnecr richer eased f inra Th ctiand on olight f heaREE, vy RE wher E [41 eas ]. Imaﬁc n thisr r ocks egarcontain d, Sc of more Sc, Cr, Co, Ni and an increased fraction of heavy REE [41]. In this regard, Sc of average average mass fraction is less than 20 mg/kg in felsic rocks but increases to 20–40 mg/kg in mass fraction is less than 20 mg/kg in felsic rocks but increases to 20–40 mg/kg in maﬁc mafic rocks, showing it to be one of the most appropriate discriminating elements [42]. In rocks, showing it to be one of the most appropriate discriminating elements [42]. In the case the case of investigated sediments and soils, Sc mass fractions were 9.56 ± 4 and 11.4 ± 4.6 of investigated sediments and soils, Sc mass fractions were 9.56 4 and 11.4 4.6 mg/kg, mg/kg, respectively, confirming the previous inference concerning the felsic origin of respectively, conﬁrming the previous inference concerning the felsic origin of Zarafshon Zarafshon valley sedimentary material. valley sedimentary material. The same finding was confirmed by discriminating Th/Co vs. La/Sc bi-plot [43] The same ﬁnding was conﬁrmed by discriminating Th/Co vs. La/Sc bi-plot [43] (Figure 5a) and ternary Sc-La-Th [7,44] diagram (Figure 5b). On both diagrams, the (Figure 5a) and ternary Sc-La-Th [7,44] diagram (Figure 5b). On both diagrams, the majority majority of Zarafshon experimental data regarding either sediments or soils are of Zarafshon experimental data regarding either sediments or soils are distributed around distributed around UCC [17] and NASC [18]. Moreover, on the Th/Co vs. La/Sc bi-plot UCC [17] and NASC [18]. Moreover, on the Th/Co vs. La/Sc bi-plot [43], all Zarafshon data [43], all Zarafshon data are closely grouped on the felsic sector of discriminating bi-plot are closely grouped on the felsic sector of discriminating bi-plot reproduced in Figure 5a. reproduced in Figure 5a. Figure 5. Discriminating bi-plots La/Th vs Hf (a) and Th/Sc vs. Zr/Sc; (b) confirming the felsic origin of Figure 5. Discriminating bi-plots La/Th vs Hf (a) and Th/Sc vs. Zr/Sc; (b) conﬁrming the fel- Zarafshon sediments and soils as well as the absence of a significant recycling of sedimentary material. sic origin of Zarafshon sediments and soils as well as the absence of a signiﬁcant recycling of sedimentary material. Two relatively closer bi-plots La/Th vs. Hf (Figure 6a) [45] and Th/Sc vs. Zr/Sc (Figure 6b) [8,46,47] provide a new type of information concerning not only the source material, Two relatively closer bi-plots La/Th vs. Hf (Figure 6a) [45] and Th/Sc vs. Zr/Sc but also the past processes that have been shaping the current position. Indeed, Hf has an (Figure 6b) [8,46,47] provide a new type of information concerning not only the source material, but also the past processes that have been shaping the current position. Indeed, Hf has an increasing tendency to be enriched during the erosion of ancient (meta) sedimentary rocks. The mineral zircon, in turn, showed to be extremely resilient during recycling, so that the higher the Zr mass fraction, the larger the sedimentary material sorting and recycling [48]. In this regard, both bi-plots conﬁrm previous inferences concerning the felsic nature of investigated sediments and soils, as well as reducing the cycle of erosion and recycling, i.e., a relatively young material. Only sediments and soils collected around the Fondarya tributary, the Kumargi Poyon, Yangob and Chore estuaries, showed a mixed felsic/basic source characterized by a higher La/Th ratio simultaneously with a reduced Appl. Sci. 2022, 12, x FOR PEER REVIEW 14 of 22 increasing tendency to be enriched during the erosion of ancient (meta) sedimentary rocks. The mineral zircon, in turn, showed to be extremely resilient during recycling, so that the higher the Zr mass fraction, the larger the sedimentary material sorting and recycling [48]. In this regard, both bi-plots confirm previous inferences concerning the felsic nature of investigated sediments and soils, as well as reducing the cycle of erosion and recycling, i.e., a relatively young material. Only sediments and soils collected around the Fondarya tributary, the Kumargi Poyon, Yangob and Chore estuaries, showed a mixed felsic/basic source characterized by a higher La/Th ratio simultaneously with a reduced Hf mass fraction. On contrary, the increased mass fraction of Hf together with reduced values of La/Th ratio suggest the presence of old sediment sources in the Mastchohi kuhi, Shahriston and some regions of Panjekent [38]. Rare Earth Elements (REE) represent a group of 17 elements, including 15 LN, Sc and Y, all of them playing a significant role in provenance studies. Traditionally, LN are classified in light LN or light REE (LREE)—La to Sm and heavy REE (HREE)—from Eu to Lu. Since REE are not easily fractionated during sedimentation, they keep the “fingerprints” of the mother rocks making them helpful in establishing their origin [48,49]. 2+ 3+ Moreover, the Eu, which can exist in two valence states (Eu and Eu ) in its bivalent state Appl. Sci. 2022, 12, 2763 13 of 21 2+ due to a smaller ionic radius, can be substituted by Sr ions in plagioclase feldspars. As this process takes place only in reducing conditions which can be found only in the superior mantle or lower crust, this leads to a distinctly negative anomaly in rocks coming Hf mass fraction. On contrary, the increased mass fraction of Hf together with reduced from the upper crust [49,50]. Another distinctive characteristic of LN, useful in evidencing values of La/Th ratio suggest the presence of old sediment sources in the Mastchohi kuhi, the rock origin, is related to the asymmetry of LREE and HREE in felsic rocks being Shahriston and some regions of Panjekent [38]. enriched in LREE with respect to mafic ones, depleted in this category of REE. Figure 6. Discriminating bi-plot Th/Co vs. La/Sc (a); and ternary Sc-La-Th diagram (b) confirming Figure 6. Discriminating bi-plot Th/Co vs. La/Sc (a); and ternary Sc-La-Th diagram (b) conﬁrming the felsic origin of investigated sediments and soils. the felsic origin of investigated sediments and soils. The La/Th ratio could be useful in inferring the provenance of sedimentary material, Rare Earth Elements (REE) represent a group of 17 elements, including 15 LN, Sc by considering that for the UCC [17] and NASC [18] this ratio is around 2.88 while in the and Y, all of them playing a signiﬁcant role in provenance studies. Traditionally, LN are case of the average Mid-Ocean Ridge Basalt (MORB) [51] it is estimated to be between 7.2 classiﬁed in light LN or light REE (LREE)—La to Sm and heavy REE (HREE)—from Eu to and 15.6. In the case of Zarafshon samples, La/Th ratios for sediments and soils were 3.23 Lu. Since REE are not easily fractionated during sedimentation, they keep the “ﬁngerprints” ± 1 and 3.03 ± 0.9, respectively (Figure 7a), both of them closer to the UCC ratio of 2.96 [17] of the mother rocks making them helpful in establishing their origin [48,49]. Moreover, 2+ 3+ and of 2.53 for NASC [18]. Further analysis of the distribution function of mass fraction of the Eu, which can exist in two valence states (Eu and Eu ) in its bivalent state due to 2+ eight REE, i.e., La, Ce, Nd, Sm, Eu, Gd, Tb, Tm and Yb, are shown to be closer to the UCC a smaller ionic radius, can be substituted by Sr ions in plagioclase feldspars. As this [16] one. This is the same peculiarity that we have noticed in the case of the La/Yb ratio, process takes place only in reducing conditions which can be found only in the superior as well as in the case of Eu negative anomaly (Figure 7b, Table3). mantle or lower crust, this leads to a distinctly negative anomaly in rocks coming from the upper crust [49,50]. Another distinctive characteristic of LN, useful in evidencing the rock origin, is related to the asymmetry of LREE and HREE in felsic rocks being enriched in LREE with respect to maﬁc ones, depleted in this category of REE. The La/Th ratio could be useful in inferring the provenance of sedimentary material, by considering that for the UCC [17] and NASC [18] this ratio is around 2.88 while in the case of the average Mid-Ocean Ridge Basalt (MORB) [51] it is estimated to be between 7.2 and 15.6. In the case of Zarafshon samples, La/Th ratios for sediments and soils were 3.23 1 and 3.03 0.9, respectively (Figure 7a), both of them closer to the UCC ratio of 2.96 [17] and of 2.53 for NASC [18]. Further analysis of the distribution function of mass fraction of eight REE, i.e., La, Ce, Nd, Sm, Eu, Gd, Tb, Tm and Yb, are shown to be closer to the UCC [16] one. This is the same peculiarity that we have noticed in the case of the La/Yb ratio, as well as in the case of Eu negative anomaly (Figure 7b, Table 3). Appl. Sci. 2022, 12, x FOR PEER REVIEW 15 of 22 Table3. The La/Sm, Gg/Yb, Eu* as well as the Th/U values for sediments and soils. For comparison, the same ratios corresponding to UCC [17] and NASC [18] are reproduced too. La/Sm Gd/Yb Eu* Th/U Sediment 4.91 ± 1.8 1.92 ± 1.3 0.69 ± 0.27 3.23 ± 1 Soils 5.81 ± 2.4 1.49 ± 1.1 0.8 ± 0.32 3.03 ± 0.9 UCC 6.6 1.9 0.72 2.96 NASC 5.56 --- --- 2.53 A possible explanation of this small discrepancy could be related to an increased U content of which average mass fraction were between 3.04 ± 1.38 mg/kg in sediments and 3.8 ± 1.5 mg/kg in soils. Appl. Sci. 2022, 12, 2763 14 of 21 These results suggest the prevalence of the felsic material and sustains the hypotheses that sediments are the main material of the Zarafshon soils. Figure 7. The La vs. Th bi-plot (a) proving that both Zarafshon sediments and soils are significantly Figure 7. The La vs. Th bi-plot (a) proving that both Zarafshon sediments and soils are signiﬁcantly closer to UCC [17] and NASC [18] than to MORB [51,52] as well as the eight REE average values of closer to UCC [17] and NASC [18] than to MORB [51,52] as well as the eight REE average values of Zarafshon sediments and soils normalized to chondrite [53] together with the corresponding UCC Zarafshon sediments and soils normalized to chondrite [53] together with the corresponding UCC data (b) [16]. data (b) [16]. 6. Conclusions Table 3. The La/Sm, Gg/Yb, Eu* as well as the Th/U values for sediments and soils. For comparison, To determine at which extent the geochemistry of Turkestan and Zarafshon ranges the same ratios corresponding to UCC [17] and NASC [18] are reproduced too. is reflected by the adjacent sedimentary material, 116 sediments, and an equal number of soil samples were collected along the Tadjik sector of Zarafshon river and its main La/Sm Gd/Yb Eu* Th/U tributaries Arthuch, Djidjikrul, Iskadardarya, Mogiyon, Sarvoda, Shing, and Yagnob. All Sediment 4.91 1.8 1.92 1.3 0.69 0.27 3.23 1 elemental analysis were performed by Instrumental Neutron Activation Analysis given Soils 5.81 2.4 1.49 1.1 0.8 0.32 3.03 0.9 its ab UCC ility to analyze ro 6.6w material, witho 1.9 ut any previo 0.72 us treatment su 2.96 ch as acid NASC 5.56 — — 2.53 dissolution. This permitted determination of mass fractions of 38 major and trace elements with a sensitivity of 1 mg/kg, in both sediments and soils samples. As for each collecting point, A possible the distance b explanation etweenof sed this ime small nts an discr d soils epancy sampcould ling wa be s no related greate to r than an incr 10eased m, it w U as content of which average mass fraction were between 3.04 1.38 mg/kg in sediments and possible to investigate the interrelationship between sediments and soils geochemistry. 3.8 1.5 All d mg/kg ata we in resoils. compared and analyzed in correlation with similar data for the Upper These results suggest the prevalence of the felsic material and sustains the hypotheses Continental Crust (UCC) and North American Shale Composite (NASC). As a general that sediments are the main material of the Zarafshon soils. conclusion, the distribution of mass fractions of all studied elements, except As, Sb and Hg showed a remarkable similarity in sediments and soils. In the case of the Presumed 6. Conclusions Contaminating Elements As, Sb and Hg, their mass fractions in few mines’ adits located To determine at which extent the geochemistry of Turkestan and Zarafshon ranges around Djidjikrut or Kanchoch tributaries exceeded two to three order of magnitude their is reﬂected by the adjacent sedimentary material, 116 sediments, and an equal number of soil samples were collected along the Tadjik sector of Zarafshon river and its main tributaries Arthuch, Djidjikrul, Iskadardarya, Mogiyon, Sarvoda, Shing, and Yagnob. All elemental analysis were performed by Instrumental Neutron Activation Analysis given its ability to analyze row material, without any previous treatment such as acid dissolution. This permitted determination of mass fractions of 38 major and trace elements with a sensitivity of 1 mg/kg, in both sediments and soils samples. As for each collecting point, the distance between sediments and soils sampling was no greater than 10 m, it was possible to investigate the interrelationship between sediments and soils geochemistry. All data were compared and analyzed in correlation with similar data for the Upper Continental Crust (UCC) and North American Shale Composite (NASC). As a general conclusion, the distribution of mass fractions of all studied elements, except As, Sb and Hg showed a remarkable similarity in sediments and soils. In the case of the Presumed Contaminating Elements As, Sb and Hg, their mass fractions in few mines’ adits located around Djidjikrut or Kanchoch tributaries exceeded two to three order of magnitude their Appl. Sci. 2022, 12, 2763 15 of 21 natural values. At the same time, mass fractions of both major and trace elements presented an increase variability characterized by coefﬁcients of variation between 15 and 200% which could be attributed to the diversity of geological formation covering the Zarafshon catchment basin. A detailed analysis of the major element oxides pointed towards a felsic origin of the collected material, with a small contribution of maﬁc one, as the alkali-silica discriminating diagrams SiO -Al O -Na O + K O + CaO suggested. At the same time, the K O-Al O -CaO 2 2 3 2 2 2 2 3 + Na O ternary diagram pointed towards a certain degree of weathering processes. Only in some places we have noticed an increased amount of magnesium and calcium oxides, most probable related to local deposits of limestone and dolomite. Relevant information was obtained by analyzing the distribution of low mobility and incompatible Sc, Zr, La, Ce, Nd, Sm, Eu, Gd, Tm, Yb as well as Th and U. Accordingly, Sc presented an average mass fraction of 10 to 11 mg/kg, characteristic of a felsic origin, a hypothesis suggested also by the reciprocal distribution of mass fractions of Sc, Co, La, Hf, or Th, in sediments as well as in soils. The la/Th vs. Hf and Th/Sc vs. Zr/Sc bi-plots suggest the absence of a signiﬁcant sorting and recycling process of sedimentary material. The REE distribution was shown to be almost identical for sediments and soils and closer to UCC and NASC. The same pattern was noticed in the case of negative Eu anomaly, which was shown to be closer to UCC and NASC. Given the surface of the investigated area which exceeds 17,700 km2, as well as the diversity of geological formation still insufﬁciently explored, the presented report should be seen as a baseline set of data for further detailed exploration. Author Contributions: Conceptualization, D.A.A. and D.A.; methodology, D.A., O.G.D. and I.Z.; software, D.A. and O.G.D.; validation, O.G.D., D.A.A. and I.Z.; formal analysis, D.A. and P.S.N.; investigation, O.G.D. and D.A.; resources, D.A.A. and O.G.D.; data curation, D.A., I.Z. and O.G.D.; writing—original draft preparation, D.A.; writing—review and editing, D.A., O.G.D., I.Z. and D.A.A.; visualization, D.A. and O.G.D.; supervision, D.A.A. and O.G.D.; project administration, D.A.A.; funding acquisition, D.A.A., I.Z. and O.G.D.; All authors have read and agreed to the published version of the manuscript. Funding: This research received no external funding. Institutional Review Board Statement: Not applicable. Informed Consent Statement: Not applicable. Data Availability Statement: All experimental data concerning sampling point coordinates, mass fraction of all 38 investigated elements are accessible at: Mendeley Reference Manager as: D.A., D.A.A., O.G.D., I.Z., P.S.N. Mendeley Data, https://doi.org/10.17632/vj24br7gnt.4 (accessed on 30 July 2021). Acknowledgments: The research was performed within the framework of the Cooperation Agree- ment between the Institute of Water Problems, Hydropower and Ecology of Academy of Sciences of Tajikistan and Sector of Neutron Activation Analysis and Applied Research of Frank Laboratory of Neutron Physics of JINR. OGD wishes to acknowledge his contribution was provided within the Cooperation Protocol no. 4920-4-20/22 between the University of Bucharest and the Joint Institute of Nuclear Research, Dubna, Russian Federation. The authors are grateful to the staff of the SNAAPI of the Frank Laboratory of Neutron Physics of JINR for carrying out the neutron activation analysis of samples. We thank two anonymous reviewers for their comments and useful suggestions. Conﬂicts of Interest: The authors declare no conﬂict of interest. Appl. Sci. 2022, 12, x FOR PEER REVIEW 17 of 22 Appl. Sci. 2022, 12, 2763 16 of 21 Appendix A Appendix A Figure Figure A1. A1. The The m mapap of Zarafshon catchm of Zarafshon catchmentent basin sho basin showingwlocations ing locations of the of the m main sour ain sou ces of anthr rces of o- anthropogenic contamination [6]. pogenic contamination [6]. Table A1. Sampling points coordinates, altitude as well as the local type of soil. Table A1. Sampling points coordinates, altitude as well as the local type of soil. Altitude Sampling Point Longitude Latitude Altitude (m) Soil Sampling Point Longitude Latitude Soil (m) Djidjikrut 1 39.109142 68.688389 2726 Regosol Djidjikrut 1 39.109142 68.688389 2726 Regosol Anzob tunnel adits 39.108853 68.687314 2703 Regosol Anzob tunnel adits 39.108853 68.687314 2703 Regosol Djidjikrut 2 39.126583 68.682944 2574 Regosol Djidjikrut 3 39.137944 68.663639 2444 Regosol Djidjikrut 2 39.126583 68.682944 2574 Regosol Djidjikrut 4 39.146806 68.651778 2398 Regosol Djidjikrut 3 39.137944 68.663639 2444 Regosol Djidjikrut 5 39.164528 68.641861 2318 Regosol Djidjikrut 4 39.146806 68.651778 2398 Regosol Djidjikrut 6 (Anzob 39.176333 68.627417 2252 Regosol Djidjikrut 5 39.164528 68.641861 2318 Regosol ore-mining combine) Djidjikrut 7 (Anzob Djidjikrut 6 (Anzob ore-mining combine) 39.176333 68.627417 2252 Regosol 39.199528 68.633278 1742 Regosol ore-mining combine) Djidjikrut 7 (Anzob ore-mining combine) 39.199528 68.633278 1742 Regosol Yagnob 1 39.217333 69.021111 2351 Regosol Yagnob 1 39.217333 69.021111 2351 Regosol Yagnob 2 39.216806 68.919333 2215 Regosol Yagnob 2 39.216806 68.919333 2215 Regosol Yagnob 3 39.172756 68.874414 2151 Regosol Yagnob 4 (before Ya Anzob gnob 3 39.172756 68.874414 2151 Regosol 39.162083 68.845222 2090 Regosol conﬂuence} Yagnob 4 (before Anzob confluence} 39.162083 68.845222 2090 Regosol Estuary of Anzob river Estuary of Anzob river to the Yagnob 39.150304 68.850006 2144 Regosol 39.150304 68.850006 2144 Regosol to the Yagnob Yagnob 5 (after Anzob confluence) 39.189667 68.758722 2070 Regosol Yagnob 5 (after Anzob 39.189667 68.758722 2070 Regosol Yagnob 6 39.192972 68.693472 1888 Regosol conﬂuence) Yagnob 6 39.192972 68.693472 1888 Regosol Yagnob 7 39.199972 68.640139 1739 Regosol Yagnob 7 39.199972 68.640139 1739 Regosol Yagnob 8 39.194278 68.598278 1706 Regosol Yagnob 8 39.194278 68.598278 1706 Regosol Yagnob 9 39.187472 68.543444 1657 Regosol Yagnob 9 39.187472 68.543444 1657 Regosol Saritag 1 39.028528 68.271278 2477 Regosol Saritag 1 39.028528 68.271278 2477 Regosol Saritag 2 Saritag 2 39.056417 3 68.346444 9.056417 68.346444 2194 2194 Regosol Regosol Konchoch 39.042167 68.332750 2361 Luvisol Kanchoch mine adit 39.039528 68.337889 2457 Luvisol Iskandardarya 1 39.101361 68.403583 2015 Regosol Iskandardarya 2 39.134028 68.453528 1820 Regosol Iskandardarya 3 (estuary of river) 39.186556 68.534944 1658 Regosol Fondarya 1 39.196389 68.536028 1644 Regosol Appl. Sci. 2022, 12, 2763 17 of 21 Table A1. Cont. Sampling Point Longitude Latitude Altitude (m) Soil Konchoch 39.042167 68.332750 2361 Luvisol Kanchoch mine adit 39.039528 68.337889 2457 Luvisol Iskandardarya 1 39.101361 68.403583 2015 Regosol Iskandardarya 2 39.134028 68.453528 1820 Regosol Iskandardarya 3 39.186556 68.534944 1658 Regosol (estuary of river) Fondarya 1 39.196389 68.536028 1644 Regosol Alovdin Lake 1 39.237642 68.254278 2780 Regosol Alovdin Lake 2 39.237472 68.261083 2780 Regosol Sarvoda 1 39.250194 68.268889 2620 Regosol Sarvoda 2 39.262944 68.310917 2488 Cambisol Sarvoda 3 39.246278 68.355750 2358 Cambisol Sarvoda 4 39.252111 68.405083 2166 Gleysol Sarvoda 5 39.226611 68.441028 1958 Gleisol Sarvoda 6 39.223194 68.484611 1808 Gleisol Sarvoda 7—estuary of 39.219889 68.527639 1660 Regosol river Fondarya 2 39.225167 68.530250 1626 Regosol Pete 1 (right tributary to 39.248639 68.561778 1895 Gleisol Fondarya) Pete 2 (right tributary to 39.249361 68.549889 1710 Gleisol Fondarya) Fondarya 3 39.258806 68.544000 1589 Regosol Kumargi Bolo 1 39.276861 68.573056 2029 Regosol Kumargi Bolo 2 39.275444 68.547583 1690 Regosol Chore 1—upper of river 39.313639 68.479694 2148 Regosol Chore 2—adit 39.308944 68.506194 1863 Regosol Chore 3—adit 39.308639 68.514056 1753 Regosol Chore 4—adit 39.308222 68.528694 1577 Regosol Chore 5—estuary of 39.306083 68.532917 1580 Regosol river Fondarya 4 39.305528 68.533861 1580 Cambisol Fondarya 5 39.344750 68.554333 1466 Cambisol Kumargi poyon 1 39.325944 68.628389 3629 Gleysol Kumargi poyon 2 39.363167 68.602694 1782 Gleysol Kumargi poyon 3 39.363967 68.561083 1434 Gleysol Fondarya 6 39.380528 68.549556 1389 Cambisol Zarafshon 1 39.452667 70.426100 2732 Regosol Zarafshon 2 (Dihisor) 39.426194 70.307583 2612 Regosol Zarafshon 3 (Dihisor) 39.444472 70.189750 2517 Regosol Zarafshon 4 (Paldorak) 39.457583 70.076194 2423 Regosol Zarafshon 5 (Paldorak) 39.426417 69.963444 2330 Regosol Zarafshon 6 (Sabak) 39.447639 69.841194 2272 Regosol Zarafshon 7 39.453167 69.723861 2267 Regosol (Madrushkat) Rovut– tributary to 39.449194 69.676306 2242 Regosol Zarafshon Zarafshon 8 39.440358 69.601324 2158 Regosol (Madrushkat) Madrushkat– tributary 39.446944 69.563472 2123 Regosol to Zarafshon Appl. Sci. 2022, 12, 2763 18 of 21 Table A1. Cont. Sampling Point Longitude Latitude Altitude (m) Soil Tributary 2—to 39.439889 69.542361 2075 Regosol Zarafshon (Isizi poyon) Zarafshon 9 Isizi poyon) 39.431222 69.483639 1999 Regosol Tributary 3—to 39.415750 69.418694 1985 Regosol Zarafshon (Isizi poyon) Zarafshon 10 (Isizi 39.413306 69.376833 1927 Regosol poyon) Zarafshon 11 (Pastigov) 39.413833 69.269194 1919 Regosol Kallakhona–tributary to 39.418194 69.264861 1913 Regosol Zarafshon Oburdon (Pastigov) 39.425611 69.167250 1875 Regosol Zarafshon 12 (Pastigov) 39.417056 69.156833 1820 Regosol Zarafshon 13 39.401222 69.060500 1742 Regosol (Shamtuch) Zarafshon 14 (Veshab) 39.402833 68.954028 1660 Regosol Zarafshon 15 (Shavadki 39.391472 68.853306 1619 Regosol poyon) Zarafshon 16 (Rarz) 39.380639 68.773361 1508 Regosol Zarafshon 17 (Fatmev) 39.385861 68.673861 1462 Regosol Zarafshon 18 39.387250 68.570250 1405 Regosol (Sangiston) Shahriston 1, tributary 39.520806 68.553389 2728 Regosol right site of tunnel Shahriston 2, tributary 39.519972 68.554889 2744 Regosol left site of tunnel Shahriston 3–estuary 39.440583 68.541389 1682 Luvisol Zarafshon 19 39.419455 68.509311 1366 Regosol Zarafshon 20 39.439194 68.441583 1306 Regosol Zarafshon 21 39.439194 68.441583 1284 Regosol Zarafshon 22 39.440806 68.273250 1226 Regosol Zarafshon 23 39.443472 68.087750 1206 Regosol Artuch 1 (Alpine camp) 39.274889 68.139167 2142 Luvisol Artuch 2 39.335278 68.087750 1573 Luvisol Artuch 3 39.397806 68.043250 1267 Regosol Zarafshon 24 39.471667 67.991833 1113 Gleysol Zarafshon 25 39.466472 67.887139 1072 Gleysol Obi Sara 1 39.379278 67.880028 1775 Regosol Obi Sara 2 39.415889 67.865639 1315 Regosol Obi Sara 3 39.468389 67.872833 1079 Regosol Zarafshon 26 39.497306 67.785056 1035 Gleysol Lake 1 39.113250 67.855250 2393 Regosol (Khazorchashma) Lake 2 (Marguzor) 39.140972 67.859528 2106 Regosol Lake 3 39.166083 67.838972 1888 Regosol Lake 4 39.197278 67.819333 1811 Regosol Lake 5 39.203564 67.810650 1718 Regosol Lake 6 39.210056 67.805028 1701 Regosol Lake 7 39.220306 67.800806 1610 Regosol Shing 1 39.240806 67.798028 1565 Regosol Shing 2 39.273667 67.802778 1382 Regosol Shing 3 industrial zone 39.306917 67.783778 1282 Regosol Mogiyon 1 39.112611 67.733639 2383 Gleysol Mogiyon 2 39.147750 67.737000 2144 Gleysol Mogiyon 3 39.215194 67.711944 1722 Gleysol Mogiyon 4 39.273722 67.688639 1474 Gleysol Mogiyon 5 39.315583 67.770167 1250 Luviysol Appl. Sci. 2022, 12, 2763 19 of 21 Table A1. Cont. Sampling Point Longitude Latitude Altitude (m) Soil Mogiyon 6 after junction with 39.339583 67.770306 1222 Regosol Shing river Mogiyon 7 39.378778 67.759472 1180 Regosol Mogiyon 8 39.419444 67.766083 1099 Regosol Mogiyon 9 39.456556 67.735889 1041 Regosol Mogiyon 10 39.495083 67.711861 994 Regosol Zarafshon 27 39.502889 67.678861 981 Regosol Zarafshon 28 39.496728 67.552247 934 Gleysol Zarafshon 29 39.529500 67.433860 883 Gleysol Table A2. The certiﬁed as well as experimentally determined mass fractions of the NIST 2709 CRM elements. Certiﬁed Measured Certiﬁed Measured Element Element (w%) (w%) (mg/kg) (mg/kg) Al 7.37 7.11 0.16 Sb 1.55 1.6 0.06 Ca 1.91 1.99 0.09 Ba 979 951 29 Fe 3.36 3.45 0.07 Cr 130 121 9.2 Mg 1.46 1.38 0.03 Co 12.8 13.6 0.3 K 2.11 2.15 0.06 Mn 529 546 19 Si 30.3 30.95 0.41 Sr 239 230 8 Na 1.22 1.26 0.03 V 110 121 11 Ti 0.34 0.3 0.01 Zr 195 201 50 Table A3. The matrix of Spearman’s correlation coefﬁcients of major elements (as oxides) in soils and sediments. All correlations signiﬁcant at p < 0.05 are represented in red (positive correlation) or blue (negative correlation) color. Sediments SiO TiO Al O FeO MnO MgO CaO K O 2 2 2 3 2 2 TiO 0.251 Al O 0.302 0.840 2 3 FeO 0.340 0.758 0.819 MnO 0.018 0.621 0.639 0.510 MgO 0.804 0.381 0.357 0.382 0.013 CaO 0.752 0.195 0.184 0.153 0.191 0.577 K O 0.155 0.612 0.627 0.728 0.392 0.268 0.260 Na O 0.204 0.419 0.410 0.276 0.313 0.066 0.435 0.262 Soils SiO TiO Al O FeO MnO MgO CaO K O 2 2 2 3 2 2 TiO 0.081 Al O 0.119 0.645 2 3 FeO 0.291 0.445 0.348 MnO 0.009 0.442 0.456 0.300 MgO 0.671 0.062 0.035 0.153 0.022 CaO 0.668 0.436 0.527 0.123 0.356 0.463 K O 0.213 0.543 0.626 0.459 0.255 0.108 0.276 Na O 0.081 0.536 0.403 0.422 0.378 0.011 0.268 0.431 References 1. Prokhorov, A.M. Zarafshon (river in Central Asia). 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DOI: 10.3390/app12062763
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Abstract

applied sciences Article On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan 1 1 , 2 2 , 3 , 4 , 2 , 5 Djamshed A. Abdushukurov , Daler Abdusamadzoda , Octavian G. Duliu * , Inga Zinicovscaia and Pavel S. Nekhoroshkov Institute of Water Problems, Hydropower and Ecology of Academy of Science, 14a Ainy Str., Dushanbe 734042, Tajikistan; abdush_dj@mail.ru (D.A.A.); martinez-91@mail.ru (D.A.) Joint Institute for Nuclear Research, 6, Joliot Curie Str., 141980 Dubna, Russia; zinikovskaia@mail.ru (I.Z.); p.nekhoroshkov@gmail.com (P.S.N.) Department of Structure of Matter, Faculty of Physics, University of Bucharest, Earth and Atmospheric Physics and Astrophysics, 405, Atomistilor Str., 077125 Magurele, Romania Geological Institute of Romania, 1, Caransebes Str., 012271 Bucharest, Romania Department of Nuclear Physics, Horia Hulubei National Institute for R&D in Physics and Nuclear Engineering, 30 Reactorului Str., P.O. Box MG-6, 077125 Magurele, Romania * Correspondence: o.duliu@upcmail.ro Abstract: To assess the geochemical features of sedimentary material of Zarafshon river, (Western Tajikistan) catchment basin, the mass fractions of 38 major and trace elements were determined by Instrumental Neutron Activation Analysis (INAA) in 2 116 paired samples of sediments and soils collected along the Zarafshon River and its main tributaries from the sources to Tajik—Uzbek border. At each collecting location, the distance between sediments and soils’ sampling was no greater Citation: Abdushukurov, D.A.; than 10 m allowing the studying of the interrelation between sediments and soils. This evidenced Abdusamadzoda, D.; Duliu, O.G.; a signiﬁcant similarity between paired soils and sediments’ samples, including the potentially Zinicovscaia, I.; Nekhoroshkov, P.S. contaminating elements As, Sb and Hg, whose mass fractions in some places were signiﬁcantly On the Geochemistry of Major and Trace Elements Distribution in higher than for the Upper Continental Crust (UCC) and North American Shale Composite (NASC), Sediments and Soils of Zarafshon suggesting a common provenience. At the same time, the distribution of major, as well as of River Valley, Western Tajikistan. Appl. incompatible trace elements, Sc, Zr, REE, Th, and U, in spite of geological diversity of the Zarafshon Sci. 2022, 12, 2763. https://doi.org/ river catchment basin, suggest a possible felsic origin of investigated material. 10.3390/app12062763 Keywords: Zarafshon; Tajikistan; sediments; soils; INAA; felsic material; REE Academic Editors: Claudia Stihi and Antoaneta Ene Received: 7 February 2022 Accepted: 3 March 2022 1. Introduction Published: 8 March 2022 The Zarafshon River originates at the Zarafshon glacier, at an altitude of 2775 m, Publisher’s Note: MDPI stays neutral at the junction of the Turkestan and Zarafshon ranges, both of them belonging to the with regard to jurisdictional claims in western sector of the Pamir-Alay system [1]. The initial part of the river, about 300 km long, published maps and institutional afﬁl- lies in a narrow, deep valley. On the southern left bank, ﬂowing between the Turkestan iations. and Zarafshon ranges, it receives the Yagnob, Arthuch and Mogiyon rivers, as well as many small tributaries (Figure 1) [1–3]. After the city of Panjakent, the river follows a ﬂat region, crosses the Tajikistan-Uzbekistan border, passes Samarkand and Bukhara, to ﬁnally disappear in the desert in the vicinity of the city of Karakul, without reaching the Copyright: © 2022 by the authors. Amu Darya River [3,4]. Its catchment basin, with an area of 17,700 km , covers diverse Licensee MDPI, Basel, Switzerland. geological formations spread from the alpine zone, 3200–3500 m above sea level, to less This article is an open access article than 150 m elevation westward towards the city of Karakul. In the Zarafshon mountain distributed under the terms and gorges, below 1500 m there are small areas of semi-savannahs as well as mountain forests. conditions of the Creative Commons Attribution (CC BY) license (https:// Here, regosols are prevalent [5], while in the western sector of Zarafshon Valley luvisols creativecommons.org/licenses/by/ formed on loess deposits are common. Moreover, in mountain gorges, terraces of alluvial 4.0/). Appl. Sci. 2022, 12, 2763. https://doi.org/10.3390/app12062763 https://www.mdpi.com/journal/applsci Appl. Sci. 2022, 12, 2763 2 of 21 Appl. Sci. 2022, 12, x FOR PEER REVIEW 3 of 22 deposits and outﬂow cones of lateral tributaries serve as the basis for soil components (Figure 1a, Table A1). Figure 1. Figure 1. The Themap of Zarafshon Valley ( map of Zarafshon Valley (a a)); ; s showing howing its po its position sition with within in Taj Tajikistan ikistan territory ( territory (b b). ). Appl. Sci. 2022, 12, 2763 3 of 21 The “Zarafshon” name, which in Farsi means “spreader of gold”, reﬂects the existence of ore ﬁelds along the river valley which, together with other outcrops of nonferrous ores makes it a mineral rich province requiring a detailed investigation. Although the total population of Zarafshon valley does not exceed 400,000 inhabitants, mainly populating small villages, the existence of non-ferrous ore outcrops could represent the main source of down-stream contamination, previously analyzed in [6]. For this reason, the distribution of major and rock-forming elements as well as of incompatible lithophile elements such as Sc, Ti, V, Cr, Zr, lanthanides (LN) Th or more soluble U together with siderophile Co and Ni were chosen for this study. All of them play a signiﬁcant role in geochemistry and pedology as tracers of the origin of natural material which, disintegrated during weathering and erosion, represents the main con- stituents of sediments and soils [7–10]. Besides them, there are other trace elements such as V, Cr, Co, Ni, Zn, As, Sb, or Hg, intensively used in diverse industrial processes, and, the presence of which, at levels signiﬁcantly exceeding the natural ones, are related to an anthropogenic contamination which could be industrial [11,12] or due to urban as well as rural agglomerations [13]. According to [14], soil is a result of the combined action of weather, geographic relief, organisms and human activity on the parent mineral sub- strate, all of them continuously interacting. The actual soil is no older than Pleistocene, i.e., 2.59 Ma almost coincident with the onset of Northern hemisphere glaciation. In turn, sediments represent a fragmented mineral substrate under the action of weathering and erosion and which is transported at long distances by the action of water, wind or ice and ﬁnally deposited. With respect to soil, sediments consist of unconsolidated clastic material with a reduced amount of organic matter. When consolidated by natural cementation processes, sediments turn into sedimentary rocks such as siltstone, sandstone, shale, etc. Both sediments and soils preserve the ﬁngerprint of the parental mineral substrate, which, under the action of external factors, evolve in a different manner. Collected from the same places and investigated in tandem, these sedimentary materials could bring a bonus of information concerning the local geochemistry as well as their interrelationship. In this regard, in the period of spring-autumn, between 2015 and 2018, the Institute of Water Problems, Hydropower and Ecology of the Academy of Science of Tajikistan organized a ﬁeld expedition to collect the most representative samples of sediments and soils from the Tajik sector of Zarafshon catching basin. For a better characterization of the soil–sediments interrelation, we collected from the same places distributed along the Zarafshon River and its main tributaries, including both sediments and soils samples (Figure 1a). In the case of presumed contaminated locations, mainly nonferrous mines and processing plants, samples were collected upstream and downstream at distances of no more than 10 to 20 m from them. This permitted the collecting of 116 sediments, as well as an equal number of soils samples to be analyzed at the Neutron Activation Analysis Section of the Frank Laboratory of Neutron Physics (FLNP) of the Joint Institute for Nuclear Research (JINR), Dubna, Russian Federation. For a better precision and accuracy, we have used the Instrumental Neutron Activation Analysis (INAA), in both its thermal and epithermal variants [15,16]. It is worth mentioning that INAA was chosen due its capacity to determine the mass fractions of up to 40 elements, 38 in the case of this study, without any preliminary processing prone to induce systematic errors (Table 1) [16]. Appl. Sci. 2022, 12, 2763 4 of 21 Table 1. The mass fraction of investigated elements in sediments and soils as well as the main literature references: UCC [17]; North American Shale Composite NASC [18]; Post Archaean Aus- tralian Shale (PAAS) [8]; Suspended Matter of the World’s Rivers (SMWR) [19]; as well as Average World Suspended Sediments (AWSS) [20]. Oxides’ mass fraction expressed in wt.%, in mg/kg for other elements, excepting Hg of which the mass fraction is expressed in g/kg. CSU represents the Combined Standard Uncertainty [21]. Element Sediment CSU Soils CSU UCC NASC PAAS SMWR AWSS SiO 62.75 12.65 59.39 9.7 66.62 64.48 62.8 54.76 54.34 TiO 0.62 0.22 0.83 1.06 0.64 0.72 1 0.65 0.73 Al O 9.9 3.52 12.92 4.07 15.4 16.9 2.2 16.31 16.48 2 3 FeO 3.79 2.5 5.78 2.01 5.04 5.7 18.9 6.47 7.47 MnO 0.07 0.07 0.09 0.03 0.1 0.06 0.11 0.15 0.22 MgO 6.32 3.42 5.8 2.72 2.48 2.85 — 2.39 2.09 CaO 10.59 10.71 9.46 9.06 3.59 3.56 1.3 3.64 3.62 K O 2.4 0.99 2.83 0.79 2.8 3.99 3.7 2.59 2.04 Na O 1.4 0.79 0.9 0.41 3.27 1.15 1.2 1.11 0.96 Sc 9.6 4 11 5 14 15 16 14 18 V 101 56 254 1500 97 — — 120 129 Cr 71 40 90 57 92 124 110 85 130 Co 11.5 6.4 14.5 7.1 17.3 — — 19 22.5 Ni 46 32 65 31 47 58 55 50 74 Zn 102 57 119 54 67 — —- 130 208 As 63 254 84 600 4.8 28.4 — 14 36.3 Br 2.6 4.3 1.9 1.6 1.6 0.9 — 9 21.5 Rb 92 41 103 39 84 126 160 77.0 79 Sr 143 63 177 100 320 142 200 150.0 187 Zr 220 133 210 101 193 200 210 150.0 160 Sb 59 560 38 270 0.4 — — 1.4 2.2 Cs 4.5 570 7.5 3.6 4.9 5.2 15 5.2 6.3 Ba 724 450 784 500 624 636 650 500 522 La 28 14 32 12 31 31 38.2 32 37 Ce 53 26 61 25 63 67 79.6 68 73.6 Nd 27 15 32 17 27 27 33.9 29 32.2 Sm 5 2.5 6.3 3.4 4.7 5.6 5.6 5.8 6.1 Eu 0.9 0.6 1.1 0.8 1 1.2 1.1 1.4 1.3 Gd 3.9 3.3 2.9 2.4 4 — 4.7 5.6 5.3 Tb 0.7 0.3 1 0.4 0.7 0.9 0.8 0.8 0.8 Tm 0.3 0.3 0.5 0.5 0.3 — 0.4 0.4 0.4 Yb 1.9 1.2 2.2 1.5 2 3.1 2.8 2.5 2.1 Hf 5.5 3 5.8 2.6 5.3 6.3 — 4.4 4 Ta 0.8 0.4 1 0.5 0.9 1.12 14.6 0.9 1.3 W 2.5 5.7 2.8 2.7 1.9 2.1 — 1.4 2 Hg 2.5 14.7 1.1 4.5 0.1 — — 0.1 — Th 8.9 4.3 10.9 3.5 10.5 12.3 3.2 10 12.1 U 3 1.5 3.9 1.7 2.7 2.7 — 2.4 3.3 2. Hypothesis and Research Objectives As presented before, the Zarafshon catchment basin covers a diversity of geological formations of which the origin dates back to Oligocene. This was when, as mentioned in [22], a Jurassic basin ﬁlled with continental sediments, under the pressure exerted by the Hindustan continental plate, and generated the Pamir-Alay system. Therefore, it is to be expected that the materials of which the Zarafshon valley is made up to contain a signiﬁcant proportion of crustal matter. In time, due to weathering, this tends to be transported by the river and its tributaries as suspended load and deposited on river beds and river banks, as the mineral constituents of soils. Accordingly, the main goals of this study consist of: (i) to verify to what extent the geochemistry of depositional material, i.e., sedi- ments and soils, can be related to crustal material, better approximated by UCC [17] Appl. Sci. 2022, 12, 2763 5 of 21 and NASC [18], PAAS [8] in the case of soils, and SMWR [19], as well as AWSS [20] for sediments; (ii) to evidence any interrelationship between the geochemistry of sediments and adjacent soils, as it is reﬂected by the distribution of major rock forming, as well as incompatible elements. It should be noted that we have paid special attention to those elements whose presence is not related to any industrial activities such as mining, as the presence and distribution of the Presumably Contaminating Elements (PCE) on the Zarafshon catchment basin were previously analyzed in [6]. The results of our study performed under these circumstances will be further presented and discussed. 3. Geological Setting Due to its location between two important mountain ranges—Turkestan and Zarafshon– the Zarafshon catchment’s basin covers a variety of lithologies of which clastic material represents the main component of sediments and bordering soils. According to [22], the actual Turkestan and Zarafshon ranges evolved during Oligocene from a Jurassic basin ﬁlled with continental, shallow-water marine and lagoonal sediments of which crustal origin seems to inﬂuence its present geochemistry. This was the main rea- son for which we have chosen UCC [17] and NASC [18] as the most appropriate descriptor of investigated material. At present, Djidjikrut, Fondarya, both tributaries of the Yagnob, as well as Mogiyon and its tributaries have the most important contribution to the mineral composition of Zarafshon sedimentary material [23,24]. The Djidjikrut River ﬂowing in the Ayni district passes through clays, marls, lime- stones, dolomites and salts, signiﬁcantly inﬂuencing the mineral composition of water and neighboring sediments and soils. At the conﬂuence with the Zarafshon (Yagnob river), is located the Djidjikrut ore ﬁeld related to Zarafshon-Gissar mercury-antimony belt, and dating to Middle and Upper Paleozoic. Antimonite, cinnabar and metacinnabarite are the main minerals of the Djidjikrut ore ﬁeld, while pyrite and marcasite with an admixture of Co, Ni, Cu, As, Sb, Au, Te and Bi, realgar and orpiment, as well as hematite and sphalerite are common minerals too. For this reason, at the conﬂuence of the Djidjikrut and Yagnob rivers, on the northern slope of the Gissar range, the Anzob mining and processing plant is operating [5] with the ﬁnal release of Hg-Sb concentrate, an important source of downstream contamination (Figure A1). The Yagnob River ﬂows westward through the narrow mountain gorge along the southern edge of the Zarafshon mountains, being the ﬁrst tributary of the Fondarya River. The total length of the Yagnob river is 114 km with a basin area of 1660 km , while the mineral composition of sediments and soils of its upper reaches is still poorly investigated. Downstream, near the conﬂuence with Fondarya, the Fon-Yagnob coal deposit occupies almost the entire left-bank site between the Djidjikrut and Pasrud tributaries [25]. Here, due to exothermic oxidation of the sub-surface coal layers, rich in pyrite and marcasite, a self-ignition process contaminated neighboring locations. Here, the paralava, a product of complete melting and (partial) recrystallization of local rocks generated by the high temperature attained during underground coal combustion, consists of almost melted sediments enclosing coal seams [26–28]. It is supposed that the underground coal ﬁre may contribute to diagenesis of some REE minerals such as godovikovite, efremovite, maskanite, and so on [27–30]. The Fondarya River with a signiﬁcant catchment basin of 3230 km is formed by the conﬂuence of the Yagnob and Iskandardarya, which then crosses the Zarafshon ridge and ﬂows into the Zarafshon river. In addition, the Fondarya is fed by the waters of the Sarvoda river which originates from the Alovdin lakes, as well as the lower and upper Kumarg tributaries, Chore and Pete (Figure 1a). Appl. Sci. 2022, 12, 2763 6 of 21 It should be noted that in the upper ﬂows of the Iskandardarya river operates the mining and processing plant “Tolko-Gold”, which extracts and processes Au, Ag, Hg, and Sb ore as well as ﬂuorite. The mining operation is also carried out at the gold deposit in the Kumargi Bolo gorge. The Chore River gorge is classiﬁed as gold-quartz deposits at the Turkestan-Chore zones of Central Tajikistan [31]. This deposit was discovered in 1960 and intensively exploited during 1974–1984 mainly for pyrite and arsenopyrite which represented more than 95% of all ore minerals together with small amounts of antimonites, chalcopyrite, sphalerite, pyrrhotite, and others [32]. The Pete tributary ﬂows between the Pete-Takfon ore ﬁeld hosting Takfon, Pete, Simich, and other deposits. In the geological structure of this ore ﬁeld, Paleozoic formations are widely developed, which are represented by Silurian (shales, limestones, dolomites with interlayers of quartzites), Devonian (siliceous and micaceous shales with interlayers of cherts and limestones), Carboniferous (limestones with horizons of clay shales, sandstones) and Cong deposits. To the south of the ore ﬁeld area, the complex of Paleozoic formations is overlapped by sub-platform sediments of the Mesozoic. The Igneous formations are represented by the Pete intrusions of granodiorites, dikes of granodiorite-porphyry, and lamprophyres. There are also tin and silver, lead, and zinc-containing ores [33]. 2, The Mogiyon river (Figure 1a), with a length of 68 km and a basin area of 1100 km is one of the largest Zarafshon tributaries. From the source to the village of Mogiyon in a narrow valley, the river ﬂows in a northern direction, cutting through the Zarafshon ridge with a deep transverse gorge. Further on, having received its largest tributary–the Shing River–it continues to ﬂow in a narrow rapids channel with a width of up to 10 m. Nine kilometers above the city of Panjakent, leaving the gorge and passing through the village of Sujina, it then falls into the Zarafshon River (Figure 1). Between the Shing and Mogiyon interﬂuve is located the Taror ore ﬁeld, which belongs to the Western Zarafshon- Gissar metallogenic zone [34]. However, along with gold-sulﬁde mineralization, silver-tin-base metal mineralization, localized in its upper and middle horizons, is also developed. The silver deposits in the Taror ore ﬁeld belong to the Mirkhant deposit and its mineralization is predominantly rep- resented by a silver-tin-polymetallic association spatially combined with sulﬁde, showing the closest correlation between Ag and Sb [27]. It is worth noting that in the Tarror gold ore deposit operates the Joint Venture “Zarafshon” whose main product consists of Ag-Au alloy [35]. In addition, along Zarafshon river and some of its main tributaries there is an active mining and metallurgical industry, based on the extraction and processing of non-ferrous metals. Among them, the Anzob mining and processing plant (AMPP), Taror gold ore plant (TGOP), Upper Kumarg and Kanchoch AGOK and TGOP specialized in the production of antimony-mercury concentrates and, respectively, gold. All of them could be regarded as a potential source of anthropogenic contamination which needs continuous monitoring extended to both the sediments and neighboring soils [35]. In this regard, the investigated Zarafshon valley together with some of its tributaries are the object of controversy between scientists and environmental experts representing governmental and non-governmental organizations. For this reason, it is not entirely correct to assess the environmental state of a particular region without paying a special attention to its geochemical features. 4. Materials and Methods 4.1. Sampling An equal number of 116 sediments and 116 soils samples were collected in the in- vestigated area (Figure 1a), using an AMS 12 Multi Stage sediments Sampler (AFMS Inc., American Falls, ID, USA) equipped with tubular glass sampler. Unconsolidated columns of sediment, 20 to 30 cm long, were handpicked from the riverbeds during a high-water period. As at altitudes greater than 2000 m, the soil cover is less developed, so that soil Appl. Sci. 2022, 12, 2763 7 of 21 columns were no longer than 10 cm. For our study we retained the top soil (horizon A), as we were also interested to evidence recent contamination processes [6]. We collected soil samples always nearby the river banks. After collecting, any traces of vegetable matter such as fragments of grass and grass roots, leaves, wood pieces, as well as fragments of rock were carefully removed. From each sampling point, three sub-samples of collected material, e.g., sediment or soil, covering an area of about 10 m were gathered and carefully mixed to form a composite sample. Any possible cross-contamination was avoided by washing the glass sampler before any sampling with a solution of diluted hydrochloric acid with deionized water and soaking them with disposable cotton serves. To evidence any correlation between sediments’ and soils’ geochemistry, sediment and soil samples were collected in the same places, with two exceptions, and the dis- tance between the sediments and the soils’ sampling location never exceeded 5–10 m (Table 1) and [36]. The same distances separated mines, adits or tunnels of the downstream collecting places. 4.2. Samples Preparation Samples consisting of silty grayish sand without organic detritus were placed into the plastic container with cooled refrigerant and kept at 4 C. In the laboratory, all samples were dried at 70 C at constant weight and ground. Finally, the dried material was sieved using a 0.425 mm (42 mesh) sieve, homogenized and sent to the Frank Laboratory of Neutron Physics (FLNP) of the Joint Institute for Nuclear Research (JINR) for further INAA. Here, 10 g of each sample were homogenized again for 15 min in a planetary ball mill (PULVERISETTE 6, Fritsch Laboratory Instruments GmbH, Idar-Oberstein, Germany) at 400 rpm. To increase the precision and accuracy of measurements, six aliquots of about 0.3 g were selected from each sample and independently analyzed. 4.3. INAA Measurements and Quality Control Before irradiation at the IBR-2 reactor of the JINR FLNP in Dubna, each aliquot was packed in polyethylene bags for the determination of short-living isotopes (three aliquots) and in aluminum foil (three aliquots) for long-living ones. It is worth mentioning that the mass fractions of short-living isotopes were determined by thermal neutron activation while in the case of long-living isotopes we have used epithermal neutrons. More details concerning irradiation time and neutron ﬂux densities in each irradiation channel can be found in [37]. After irradiation, the gamma spectrum of each sample was recorded using a HPGe detector with a resolution of 1.9 keV for the Co 1332 keV line, analyzed by means of a Genie 2000 Canberra software and processed by a proprietary software [37]. This permitted determination of the mass fraction of each of the 38 considered elements together with the associated CSU [21]. In all cases, the CSU was estimated by taking into account the statistical error, inﬂuence of measurement geometry, detector efﬁciency, the content, as well as the error of each element for all Certiﬁed Standard Material (CSM) utilized for calibration. To avoid any environmental contamination, all resulting radioactive materials were deposited in a permanent low activity repository. The quality control was assured in the case of sediments and soils by a simultane- ous analysis of Standard Reference Materials (SRM) provided by the National Institute for Standard and Technologies (NIST), i.e., 1633c Coal ﬂy ash, 667 Estuarine sediment, 2710 Montana Soil and 1547 Peach leaves for short half-life time isotopes. In the case of long life-time isotopes, the best results were obtained using–2709 Trace elements in soil, 1632c–Trace elements in coal, 690CC–Calcareous soil, 2709a–San Joaquin soil, 1632c–Trace elements in coal and SRM-AGV2–Andesite. Further, by using all of the above-mentioned SRM a Group of Standard Sample (GSS) [37,38] was realized which permitted the choice of the most appropriate SRM lines to minimize errors in determining the mass fractions of all investigated elements. It is worth Appl. Sci. 2022, 12, 2763 8 of 21 mentioning that GSS is a proprietary software which, besides helping to determine the mass fractions of chosen elements, it allowed the calculation of the extent to which the mass fractions of SRM corresponded to certiﬁed ones [37,38]. Following this procedure, the accuracy quantiﬁed by means of standard deviation corresponding to each group of three aliquots was lower than 10%. In the case of SRM, the CSU varied between 3 and 15%, higher in the case of REE, but never greater than 20%. It is worth mentioning that for all 38 investigated elements, the detection limit was of 1 mg/kg and lower [37,38]. To illustrate the sensitivity and accuracy of INAA measurements following the CSS software, in Table A2 we have reproduced, as an example, the experimentally determined mass fractions of SRM 2709. Similar determinations were completed in the case of all utilized SRM. 5. Results and Discussion A complete set of data concerning the mass fractions of all 38 elements in the investi- gated samples are provided in the Mendeley repository [36], while Table 1 reproduces only the mass fractions’ average values together with corresponding values of the UCC [17], NASC [18], PAAS [8], SMWR [19], as well as AWSS [20]. In interpreting compositional data of river sediments and adjacent soils, the geochem- istry of local formations usually plays a determinant role. Additionally, due to a variable mobility, different mineral fractions are mixed and deposited along river beds depending on water speed, grain sizes and speciﬁc gravity. In this regard, Figure 2 illustrates the mass fractions of investigated elements in sediments normalized to UCC (Figure 2) [16], and in soils normalized to SMWR (Figure 2) [19]. The UCC [17] was chosen as an appropriate descriptor of the continental crust, while SMWR [19] drew on the lithogenesis theory [39], according to which, the mobilization of suspended and dissolved materials in drainage basins represent the initial stage of pedogenesis. Here, a signiﬁcant fraction of chemical elements including highly mobile alkaline and calc-alkaline ones were transported as suspended sediments and deposited along river beds and banks. Therefore, other descriptors such as NASC [17], AWSS [19] or PAAS [8] showed to be almost identical. According to Table 1 and [36], the elemental composition of sediments and soils appears, excepting chalcophile Zn, As, Sb ad Hg, closer to UCC [17] and SMWR [19]. After a careful analysis of the experimental data presented in [36], mass fractions of potentially contaminating elements As, Sb and Hg showed increased values only for samples collected in the vicinity of mines and adits located on the Djidjikrut, Kanchoch, Chore and Mogiyon tributaries (Figures 1a, 2 and A1). This ﬁnding is well evidenced in Figure 3a, where the As, Sb and Hg standard devi- ations appear disproportionately high due to the fact that in a very few places, such as mines or mine adits, their mass fractions exceeded the UCC [17] one by two to three orders of magnitude. Excepting these, the average mass fractions of investigated elements were shown to be relatively closer in both sediments and soils, as suggested by ANOVA analysis (Table 2) and by both biplots reproduced in Figure 3. In addition, a Spearman’s correlation coefﬁcient of 0.83 sustains this observation (Figure 3b). Appl. Sci. 2022, 12, x FOR PEER REVIEW 10 of 22 Appl. Sci. 2022, 12, 2763 9 of 21 Figure 2. Box-plots illustrating the distribution of investigated elements in Zarafshon sediments Figure 2. Box-plots illustrating the distribution of investigated elements in Zarafshon sediments (lower); and soils (upper). All mass fractions of soils normalized to UCC [17] and sediments to (lower); and soils (upper). All mass fractions of soils normalized to UCC [17] and sediments to SMWR [19]. The values corresponding to As and Hg are divided by 10 and by 100 in the case of Sb. SMWR [19]. The values corresponding to As and Hg are divided by 10 and by 100 in the case of Sb. Appl. Sci. 2022, 12, x FOR PEER REVIEW 11 of 22 This finding is well evidenced in Figure 3a, where the As, Sb and Hg standard deviations appear disproportionately high due to the fact that in a very few places, such as mines or mine adits, their mass fractions exceeded the UCC [17] one by two to three orders of magnitude. Excepting these, the average mass fractions of investigated elements were shown to be relatively closer in both sediments and soils, as suggested by ANOVA Appl. Sci. 2022, 12, 2763 10 of 21 analysis (Table 2) and by both biplots reproduced in Figure 3. In addition, a Spearman’s correlation coefficient of 0.83 sustains this observation (Figure 3b). Figure 3. The sediment to soil ratio of mass fractions of investigated elements (red line) as well as Figure 3. The sediment to soil ratio of mass fractions of investigated elements (red line) as well as the corresponding standard deviation (gray background) (a); and a biplot illustrating the reciprocal the corresponding standard deviation (gray background) (a); and a biplot illustrating the reciprocal distribution of investigated elements in sediments and soils excepting the Zn, As, Sb and Hg, i.e., distribution of investigated elements in sediments and soils excepting the Zn, As, Sb and Hg, i.e., elements whose mass fractions in some places exceeds the UCC [17] ones by two to three orders of elements whose mass fractions in some places exceeds the UCC [17] ones by two to three orders of magnitude (b) (Table 1) [36]. Spearman’s correlation coefficient of 0.837 at p < 0.01. magnitude (b) (Table 1) [36]. Spearman’s correlation coefﬁcient of 0.837 at p < 0.01. Table 2. The results of two-sample ANOVA tests illustrating the probability the major and trace Table 2. The results of two-sample ANOVA tests illustrating the probability the major and trace elements being closer in soils and sediments. The results are based on the average mass fractions elements being closer in soils and sediments. The results are based on the average mass fractions values reproduced in Table 1. values reproduced in Table 1. ANOVA Two-Sample Test T-Test F-Test Mann–Whitney Anderson–Darling ANOVA Two-Sample Test Elements Equal Mean Equal Variance Equal Median Equal Distribution T -Test F-Test Mann–Whitney Anderson–Darling Elements Equal Mean Equal Variance Equal Median Equal Distribution Major elements 0.99 0.87 1.00 1.00 Trace elements 0.77 0.59 0.73 0.97 Major elements 0.99 0.87 1.00 1.00 Trace elements 0.77 0.59 0.73 0.97 Major elements: SiO2, TiO2, Al2O3, FeO, MnO2, MgO, CaO, K2O, Na2O Trace elements: Sc, V, Cr, Co, Ni, Zn, As, Br, Rb, Sr, Zr, Sb, Cs, Ba, La, Ce, Nd, Sm, Eu, Gd, Tb, Tm, Yb, Hf, Ta, W, Hg, Th, U Major elements: SiO TiO Al O FeO, MnO MgO, CaO, K O, Na O 2, 2, 2 3, 2, 2 2 Trace elements: Sc, V, Cr, Co, Ni, Zn, As, Br, Rb, Sr, Zr, Sb, Cs, Ba, La, Ce, Nd, Sm, Eu, Gd, Tb, Tm, Yb, Hf, Ta, W, Hg, Th, U Figure 3a evidenced also that the ratio between the same elements in sediments and soil slightly varies around one, excepting the above mentioned PCE As, Sb and Hg and, Figure 3a evidenced also that the ratio between the same elements in sediments and soil to a slightly lesser ex varies tent, Na o around f whone, ich the excepting average ma the s above s fraction was mentioned sligh PCE tly highe As, Sb r in and seHg diments and, to than a lesser in soiextent, ls, as wNa ill be of di which scusse the d in average the next s mass ection. fraction was slightly higher in sediments than in soils, as will be discussed in the next section. 5.1. Major Elements 5.1. Major Elements The average values of the mass fractions of major, rock-forming elements excepting The average values of the mass fractions of major, rock-forming elements excepting for MgO and CaO showed to be relatively closer to UCC [17], NASC, [18], PAAS [8], or for MgO and CaO showed to be relatively closer to UCC [17], NASC, [18], PAAS [8], or other sedimentary systems such as SMWR [19], or Average World Suspended Sediments other sedimentary systems such as SMWR [19], or Average World Suspended Sediments AWSS [20] (Table 1). AWSS [20] (Table 1). Silica represents the major constituent of all investigated samples, its mass fraction Silica represents the major constituent of all investigated samples, its mass fraction of 34.64 wt.% to 84 wt.% (62.8 ± 11.9 wt.% average) for sediments and of 31.53 wt.% to of 34.64 wt.% to 84 wt.% (62.8 11.9 wt.% average) for sediments and of 31.53 wt.% to 75.12 wt.% (59.4 8.8 wt.% average) for soils. On discriminating diagrams Na O + K O vs. 2 2 SiO (Figure 4a), SiO -Al O -Na O + K O + CaO (Figure 4b) and K O-Al O -Na O + CaO 2 2 2 3 2 2 2 2 3 2 (Figure 4c) the composition of investigated materials points towards a somewhat felsic to intermediate origin with a small contribution of maﬁc material as was the case in the Pete intrusion [5,24] (Table 1). Its average mass fraction was closer to the UCC [17] but with only a few exceptions in the sediments collected in the vicinity of the Anzob tunnel, Sarvoda 1, and Sarvoda 2 as well as soils from Chore 1 and 3, Djidjikrut 1, Obi Sara 1, Saritag 2, as well Appl. Sci. 2022, 12, x FOR PEER REVIEW 12 of 22 75.12 wt.% (59.4 ± 8.8 wt.% average) for soils. On discriminating diagrams Na2O + K2O vs SiO2 (Figure 4a), SiO2-Al2O3-Na2O + K2O + CaO (Figure 4b) and K2O-Al2O3-Na2O + CaO (Figure 4c) the composition of investigated materials points towards a somewhat felsic to intermediate origin with a small contribution of mafic material as was the case in the Pete Appl. Sci. 2022, 12, 2763 11 of 21 intrusion [5,24] (Table 1). Its average mass fraction was closer to the UCC [17] but with only a few exceptions in the sediments collected in the vicinity of the Anzob tunnel, Sarvoda 1, and Sarvoda 2 as well as soils from Chore 1 and 3, Djidjikrut 1, Obi Sara 1, Saritag 2, as well as Sarvoda 1 to Sarvoda 7 (Figures 1a and A1). In all locations, the lower as Sarvoda 1 to Sarvoda 7 (Figures 1a and A1). In all locations, the lower content of silica content of silica is due to an increased content of calcium oxide of which mass fractions is due to an increased content of calcium oxide of which mass fractions varied between varied between 26 and 47 wt.% (Table 1). 26 and 47 wt.% (Table 1). Figure Figure 4. 4. Discriminating Discriminating total total alkali alkali m metal etal ox oxides ides vs. vs.SiO SiO2biplot biplot( ( aa );)ternary ; ternary SiO SiO -Al 2-AlO 2O3 -Na -Na2O O + + K K 2O O 2 2 2 3 2 2 + CaO (b); and K-A-CN (c) diagrams illustrating the preponderance of felsic material in Zarafshon + CaO (b); and K-A-CN (c) diagrams illustrating the preponderance of felsic material in Zarafshon sediments and soils as well as a small fraction of weathered material. sediments and soils as well as a small fraction of weathered material. Aluminum Aluminum o oxide xide showe showed d in sed in sediments iments an an av average erage mass mass frac fraction tion 9.91 9.91 ± 3 3.2 .2 wt.%, wt.%, smaller than the soils’ one of 12.92 3.7 wt.%, both of them lower than the UCC [17] smaller than the soils’ one of 12.92 ± 3.7 wt.%, both of them lower than the UCC [17] and and NASC [17] (Table 1). At the same time, the sodium oxide has an average mass NASC [17] (Table 1). At the same time, the sodium oxide has an average mass fraction in fraction in sediments and especially in soils smaller than the corresponding UCC [17] sediments and especially in soils smaller than the corresponding UCC [17] (Table 1), (Table 1), suggesting a low content of plagioclase, and by consequence predominance of suggesting a low content of plagioclase, and by consequence predominance of a a sedimentary substrate (Figure 4a,b). This ﬁnding is illustrated by the discriminating sedimentary substrate (Figure 4a,b). This finding is illustrated by the discriminating diagram SiO -Al O -Na O + K O + CaO (Figure 4b) where some points are shifted towards 2 2 3 2 2 lower SiO content, which could be due to an increased content of CaO whose mass fraction in some places reached 28% [36]. It is worth remarking that CaO correlates positively only with MgO, in sediments as well as in soils (Table A3), suggesting the presence of dolomite CaMg(CO ) . Besides these, the K-A-CN ternary diagram suggests a weak inﬂuence of 3 2 weathering on both sediments and soils, expressed by a reduced fraction of total alkali–calc- alkali oxides Na O + CaO of which normalized values appear smaller than 0.25 (Figure 4c). 2 Appl. Sci. 2022, 12, x FOR PEER REVIEW 13 of 22 diagram SiO2-Al2O3-Na2O + K2O + CaO (Figure 4b) where some points are shifted towards lower SiO2 content, which could be due to an increased content of CaO whose mass fraction in some places reached 28% [36]. It is worth remarking that CaO correlates positively only with MgO, in sediments as well as in soils (Table A3), suggesting the presence of dolomite CaMg(CO₃)₂. Besides these, the K-A-CN ternary diagram suggests a weak influence of weathering on both sediments and soils, expressed by a reduced fraction of total alkali–calc-alkali oxides Na2O + CaO of which normalized values appear smaller than Appl. Sci. 2022, 12, 2763 12 of 21 0.25 (Figure 4c). The mass fractions of the other major elements oxides, i.e., TiO2, FeO, and MnO were closer to the UCC [17] values in conformity with the previous suppositions concerning a The mass fractions of the other major elements oxides, i.e., TiO , FeO, and MnO were rather felsic origin of investigated material (Table 1). closer to the UCC [17] values in conformity with the previous suppositions concerning a rather felsic origin of investigated material (Table 1). 5.2. Trace Elements 5.2. Trace Elements More data concerning the origin of investigated sedimentary materials can be inferr Mor ed ana e data lyzin concerning g the dist the ribu origin tion oof f tr investigated ace elements sedimentary and especially, materi as men als can tion bee inferr d in the ed analyzing Introducti the on, distribution of those cons ofitrace dered in elements compat and ible especially and insolub , as mentioned le such as in Sc, Zr, the Intr La oduction, , Ce, Nd, Sm, Eu, Gd, Tm, Yb, Th as well as U and, to a lower extent, Cr and Ni [6,7,40]. of those considered incompatible and insoluble such as Sc, Zr, La, Ce, Nd, Sm, Eu, Gd, Tm, Yb, Th Notably as well, th ase felsic rocks U and, to a lower are richer extent, in Th Cr and and ligh Ni [6t ,7 RE ,40 E, where ]. as mafic rocks contain more Notably Sc, Cr,, the Co, N felsic i an rocks d an i arnecr richer eased f inra Th ctiand on olight f heaREE, vy RE wher E [41 eas ]. Imaﬁc n thisr r ocks egarcontain d, Sc of more Sc, Cr, Co, Ni and an increased fraction of heavy REE [41]. In this regard, Sc of average average mass fraction is less than 20 mg/kg in felsic rocks but increases to 20–40 mg/kg in mass fraction is less than 20 mg/kg in felsic rocks but increases to 20–40 mg/kg in maﬁc mafic rocks, showing it to be one of the most appropriate discriminating elements [42]. In rocks, showing it to be one of the most appropriate discriminating elements [42]. In the case the case of investigated sediments and soils, Sc mass fractions were 9.56 ± 4 and 11.4 ± 4.6 of investigated sediments and soils, Sc mass fractions were 9.56 4 and 11.4 4.6 mg/kg, mg/kg, respectively, confirming the previous inference concerning the felsic origin of respectively, conﬁrming the previous inference concerning the felsic origin of Zarafshon Zarafshon valley sedimentary material. valley sedimentary material. The same finding was confirmed by discriminating Th/Co vs. La/Sc bi-plot [43] The same ﬁnding was conﬁrmed by discriminating Th/Co vs. La/Sc bi-plot [43] (Figure 5a) and ternary Sc-La-Th [7,44] diagram (Figure 5b). On both diagrams, the (Figure 5a) and ternary Sc-La-Th [7,44] diagram (Figure 5b). On both diagrams, the majority majority of Zarafshon experimental data regarding either sediments or soils are of Zarafshon experimental data regarding either sediments or soils are distributed around distributed around UCC [17] and NASC [18]. Moreover, on the Th/Co vs. La/Sc bi-plot UCC [17] and NASC [18]. Moreover, on the Th/Co vs. La/Sc bi-plot [43], all Zarafshon data [43], all Zarafshon data are closely grouped on the felsic sector of discriminating bi-plot are closely grouped on the felsic sector of discriminating bi-plot reproduced in Figure 5a. reproduced in Figure 5a. Figure 5. Discriminating bi-plots La/Th vs Hf (a) and Th/Sc vs. Zr/Sc; (b) confirming the felsic origin of Figure 5. Discriminating bi-plots La/Th vs Hf (a) and Th/Sc vs. Zr/Sc; (b) conﬁrming the fel- Zarafshon sediments and soils as well as the absence of a significant recycling of sedimentary material. sic origin of Zarafshon sediments and soils as well as the absence of a signiﬁcant recycling of sedimentary material. Two relatively closer bi-plots La/Th vs. Hf (Figure 6a) [45] and Th/Sc vs. Zr/Sc (Figure 6b) [8,46,47] provide a new type of information concerning not only the source material, Two relatively closer bi-plots La/Th vs. Hf (Figure 6a) [45] and Th/Sc vs. Zr/Sc but also the past processes that have been shaping the current position. Indeed, Hf has an (Figure 6b) [8,46,47] provide a new type of information concerning not only the source material, but also the past processes that have been shaping the current position. Indeed, Hf has an increasing tendency to be enriched during the erosion of ancient (meta) sedimentary rocks. The mineral zircon, in turn, showed to be extremely resilient during recycling, so that the higher the Zr mass fraction, the larger the sedimentary material sorting and recycling [48]. In this regard, both bi-plots conﬁrm previous inferences concerning the felsic nature of investigated sediments and soils, as well as reducing the cycle of erosion and recycling, i.e., a relatively young material. Only sediments and soils collected around the Fondarya tributary, the Kumargi Poyon, Yangob and Chore estuaries, showed a mixed felsic/basic source characterized by a higher La/Th ratio simultaneously with a reduced Appl. Sci. 2022, 12, x FOR PEER REVIEW 14 of 22 increasing tendency to be enriched during the erosion of ancient (meta) sedimentary rocks. The mineral zircon, in turn, showed to be extremely resilient during recycling, so that the higher the Zr mass fraction, the larger the sedimentary material sorting and recycling [48]. In this regard, both bi-plots confirm previous inferences concerning the felsic nature of investigated sediments and soils, as well as reducing the cycle of erosion and recycling, i.e., a relatively young material. Only sediments and soils collected around the Fondarya tributary, the Kumargi Poyon, Yangob and Chore estuaries, showed a mixed felsic/basic source characterized by a higher La/Th ratio simultaneously with a reduced Hf mass fraction. On contrary, the increased mass fraction of Hf together with reduced values of La/Th ratio suggest the presence of old sediment sources in the Mastchohi kuhi, Shahriston and some regions of Panjekent [38]. Rare Earth Elements (REE) represent a group of 17 elements, including 15 LN, Sc and Y, all of them playing a significant role in provenance studies. Traditionally, LN are classified in light LN or light REE (LREE)—La to Sm and heavy REE (HREE)—from Eu to Lu. Since REE are not easily fractionated during sedimentation, they keep the “fingerprints” of the mother rocks making them helpful in establishing their origin [48,49]. 2+ 3+ Moreover, the Eu, which can exist in two valence states (Eu and Eu ) in its bivalent state Appl. Sci. 2022, 12, 2763 13 of 21 2+ due to a smaller ionic radius, can be substituted by Sr ions in plagioclase feldspars. As this process takes place only in reducing conditions which can be found only in the superior mantle or lower crust, this leads to a distinctly negative anomaly in rocks coming Hf mass fraction. On contrary, the increased mass fraction of Hf together with reduced from the upper crust [49,50]. Another distinctive characteristic of LN, useful in evidencing values of La/Th ratio suggest the presence of old sediment sources in the Mastchohi kuhi, the rock origin, is related to the asymmetry of LREE and HREE in felsic rocks being Shahriston and some regions of Panjekent [38]. enriched in LREE with respect to mafic ones, depleted in this category of REE. Figure 6. Discriminating bi-plot Th/Co vs. La/Sc (a); and ternary Sc-La-Th diagram (b) confirming Figure 6. Discriminating bi-plot Th/Co vs. La/Sc (a); and ternary Sc-La-Th diagram (b) conﬁrming the felsic origin of investigated sediments and soils. the felsic origin of investigated sediments and soils. The La/Th ratio could be useful in inferring the provenance of sedimentary material, Rare Earth Elements (REE) represent a group of 17 elements, including 15 LN, Sc by considering that for the UCC [17] and NASC [18] this ratio is around 2.88 while in the and Y, all of them playing a signiﬁcant role in provenance studies. Traditionally, LN are case of the average Mid-Ocean Ridge Basalt (MORB) [51] it is estimated to be between 7.2 classiﬁed in light LN or light REE (LREE)—La to Sm and heavy REE (HREE)—from Eu to and 15.6. In the case of Zarafshon samples, La/Th ratios for sediments and soils were 3.23 Lu. Since REE are not easily fractionated during sedimentation, they keep the “ﬁngerprints” ± 1 and 3.03 ± 0.9, respectively (Figure 7a), both of them closer to the UCC ratio of 2.96 [17] of the mother rocks making them helpful in establishing their origin [48,49]. Moreover, 2+ 3+ and of 2.53 for NASC [18]. Further analysis of the distribution function of mass fraction of the Eu, which can exist in two valence states (Eu and Eu ) in its bivalent state due to 2+ eight REE, i.e., La, Ce, Nd, Sm, Eu, Gd, Tb, Tm and Yb, are shown to be closer to the UCC a smaller ionic radius, can be substituted by Sr ions in plagioclase feldspars. As this [16] one. This is the same peculiarity that we have noticed in the case of the La/Yb ratio, process takes place only in reducing conditions which can be found only in the superior as well as in the case of Eu negative anomaly (Figure 7b, Table3). mantle or lower crust, this leads to a distinctly negative anomaly in rocks coming from the upper crust [49,50]. Another distinctive characteristic of LN, useful in evidencing the rock origin, is related to the asymmetry of LREE and HREE in felsic rocks being enriched in LREE with respect to maﬁc ones, depleted in this category of REE. The La/Th ratio could be useful in inferring the provenance of sedimentary material, by considering that for the UCC [17] and NASC [18] this ratio is around 2.88 while in the case of the average Mid-Ocean Ridge Basalt (MORB) [51] it is estimated to be between 7.2 and 15.6. In the case of Zarafshon samples, La/Th ratios for sediments and soils were 3.23 1 and 3.03 0.9, respectively (Figure 7a), both of them closer to the UCC ratio of 2.96 [17] and of 2.53 for NASC [18]. Further analysis of the distribution function of mass fraction of eight REE, i.e., La, Ce, Nd, Sm, Eu, Gd, Tb, Tm and Yb, are shown to be closer to the UCC [16] one. This is the same peculiarity that we have noticed in the case of the La/Yb ratio, as well as in the case of Eu negative anomaly (Figure 7b, Table 3). Appl. Sci. 2022, 12, x FOR PEER REVIEW 15 of 22 Table3. The La/Sm, Gg/Yb, Eu* as well as the Th/U values for sediments and soils. For comparison, the same ratios corresponding to UCC [17] and NASC [18] are reproduced too. La/Sm Gd/Yb Eu* Th/U Sediment 4.91 ± 1.8 1.92 ± 1.3 0.69 ± 0.27 3.23 ± 1 Soils 5.81 ± 2.4 1.49 ± 1.1 0.8 ± 0.32 3.03 ± 0.9 UCC 6.6 1.9 0.72 2.96 NASC 5.56 --- --- 2.53 A possible explanation of this small discrepancy could be related to an increased U content of which average mass fraction were between 3.04 ± 1.38 mg/kg in sediments and 3.8 ± 1.5 mg/kg in soils. Appl. Sci. 2022, 12, 2763 14 of 21 These results suggest the prevalence of the felsic material and sustains the hypotheses that sediments are the main material of the Zarafshon soils. Figure 7. The La vs. Th bi-plot (a) proving that both Zarafshon sediments and soils are significantly Figure 7. The La vs. Th bi-plot (a) proving that both Zarafshon sediments and soils are signiﬁcantly closer to UCC [17] and NASC [18] than to MORB [51,52] as well as the eight REE average values of closer to UCC [17] and NASC [18] than to MORB [51,52] as well as the eight REE average values of Zarafshon sediments and soils normalized to chondrite [53] together with the corresponding UCC Zarafshon sediments and soils normalized to chondrite [53] together with the corresponding UCC data (b) [16]. data (b) [16]. 6. Conclusions Table 3. The La/Sm, Gg/Yb, Eu* as well as the Th/U values for sediments and soils. For comparison, To determine at which extent the geochemistry of Turkestan and Zarafshon ranges the same ratios corresponding to UCC [17] and NASC [18] are reproduced too. is reflected by the adjacent sedimentary material, 116 sediments, and an equal number of soil samples were collected along the Tadjik sector of Zarafshon river and its main La/Sm Gd/Yb Eu* Th/U tributaries Arthuch, Djidjikrul, Iskadardarya, Mogiyon, Sarvoda, Shing, and Yagnob. All Sediment 4.91 1.8 1.92 1.3 0.69 0.27 3.23 1 elemental analysis were performed by Instrumental Neutron Activation Analysis given Soils 5.81 2.4 1.49 1.1 0.8 0.32 3.03 0.9 its ab UCC ility to analyze ro 6.6w material, witho 1.9 ut any previo 0.72 us treatment su 2.96 ch as acid NASC 5.56 — — 2.53 dissolution. This permitted determination of mass fractions of 38 major and trace elements with a sensitivity of 1 mg/kg, in both sediments and soils samples. As for each collecting point, A possible the distance b explanation etweenof sed this ime small nts an discr d soils epancy sampcould ling wa be s no related greate to r than an incr 10eased m, it w U as content of which average mass fraction were between 3.04 1.38 mg/kg in sediments and possible to investigate the interrelationship between sediments and soils geochemistry. 3.8 1.5 All d mg/kg ata we in resoils. compared and analyzed in correlation with similar data for the Upper These results suggest the prevalence of the felsic material and sustains the hypotheses Continental Crust (UCC) and North American Shale Composite (NASC). As a general that sediments are the main material of the Zarafshon soils. conclusion, the distribution of mass fractions of all studied elements, except As, Sb and Hg showed a remarkable similarity in sediments and soils. In the case of the Presumed 6. Conclusions Contaminating Elements As, Sb and Hg, their mass fractions in few mines’ adits located To determine at which extent the geochemistry of Turkestan and Zarafshon ranges around Djidjikrut or Kanchoch tributaries exceeded two to three order of magnitude their is reﬂected by the adjacent sedimentary material, 116 sediments, and an equal number of soil samples were collected along the Tadjik sector of Zarafshon river and its main tributaries Arthuch, Djidjikrul, Iskadardarya, Mogiyon, Sarvoda, Shing, and Yagnob. All elemental analysis were performed by Instrumental Neutron Activation Analysis given its ability to analyze row material, without any previous treatment such as acid dissolution. This permitted determination of mass fractions of 38 major and trace elements with a sensitivity of 1 mg/kg, in both sediments and soils samples. As for each collecting point, the distance between sediments and soils sampling was no greater than 10 m, it was possible to investigate the interrelationship between sediments and soils geochemistry. All data were compared and analyzed in correlation with similar data for the Upper Continental Crust (UCC) and North American Shale Composite (NASC). As a general conclusion, the distribution of mass fractions of all studied elements, except As, Sb and Hg showed a remarkable similarity in sediments and soils. In the case of the Presumed Contaminating Elements As, Sb and Hg, their mass fractions in few mines’ adits located around Djidjikrut or Kanchoch tributaries exceeded two to three order of magnitude their Appl. Sci. 2022, 12, 2763 15 of 21 natural values. At the same time, mass fractions of both major and trace elements presented an increase variability characterized by coefﬁcients of variation between 15 and 200% which could be attributed to the diversity of geological formation covering the Zarafshon catchment basin. A detailed analysis of the major element oxides pointed towards a felsic origin of the collected material, with a small contribution of maﬁc one, as the alkali-silica discriminating diagrams SiO -Al O -Na O + K O + CaO suggested. At the same time, the K O-Al O -CaO 2 2 3 2 2 2 2 3 + Na O ternary diagram pointed towards a certain degree of weathering processes. Only in some places we have noticed an increased amount of magnesium and calcium oxides, most probable related to local deposits of limestone and dolomite. Relevant information was obtained by analyzing the distribution of low mobility and incompatible Sc, Zr, La, Ce, Nd, Sm, Eu, Gd, Tm, Yb as well as Th and U. Accordingly, Sc presented an average mass fraction of 10 to 11 mg/kg, characteristic of a felsic origin, a hypothesis suggested also by the reciprocal distribution of mass fractions of Sc, Co, La, Hf, or Th, in sediments as well as in soils. The la/Th vs. Hf and Th/Sc vs. Zr/Sc bi-plots suggest the absence of a signiﬁcant sorting and recycling process of sedimentary material. The REE distribution was shown to be almost identical for sediments and soils and closer to UCC and NASC. The same pattern was noticed in the case of negative Eu anomaly, which was shown to be closer to UCC and NASC. Given the surface of the investigated area which exceeds 17,700 km2, as well as the diversity of geological formation still insufﬁciently explored, the presented report should be seen as a baseline set of data for further detailed exploration. Author Contributions: Conceptualization, D.A.A. and D.A.; methodology, D.A., O.G.D. and I.Z.; software, D.A. and O.G.D.; validation, O.G.D., D.A.A. and I.Z.; formal analysis, D.A. and P.S.N.; investigation, O.G.D. and D.A.; resources, D.A.A. and O.G.D.; data curation, D.A., I.Z. and O.G.D.; writing—original draft preparation, D.A.; writing—review and editing, D.A., O.G.D., I.Z. and D.A.A.; visualization, D.A. and O.G.D.; supervision, D.A.A. and O.G.D.; project administration, D.A.A.; funding acquisition, D.A.A., I.Z. and O.G.D.; All authors have read and agreed to the published version of the manuscript. Funding: This research received no external funding. Institutional Review Board Statement: Not applicable. Informed Consent Statement: Not applicable. Data Availability Statement: All experimental data concerning sampling point coordinates, mass fraction of all 38 investigated elements are accessible at: Mendeley Reference Manager as: D.A., D.A.A., O.G.D., I.Z., P.S.N. Mendeley Data, https://doi.org/10.17632/vj24br7gnt.4 (accessed on 30 July 2021). Acknowledgments: The research was performed within the framework of the Cooperation Agree- ment between the Institute of Water Problems, Hydropower and Ecology of Academy of Sciences of Tajikistan and Sector of Neutron Activation Analysis and Applied Research of Frank Laboratory of Neutron Physics of JINR. OGD wishes to acknowledge his contribution was provided within the Cooperation Protocol no. 4920-4-20/22 between the University of Bucharest and the Joint Institute of Nuclear Research, Dubna, Russian Federation. The authors are grateful to the staff of the SNAAPI of the Frank Laboratory of Neutron Physics of JINR for carrying out the neutron activation analysis of samples. We thank two anonymous reviewers for their comments and useful suggestions. Conﬂicts of Interest: The authors declare no conﬂict of interest. Appl. Sci. 2022, 12, x FOR PEER REVIEW 17 of 22 Appl. Sci. 2022, 12, 2763 16 of 21 Appendix A Appendix A Figure Figure A1. A1. The The m mapap of Zarafshon catchm of Zarafshon catchmentent basin sho basin showingwlocations ing locations of the of the m main sour ain sou ces of anthr rces of o- anthropogenic contamination [6]. pogenic contamination [6]. Table A1. Sampling points coordinates, altitude as well as the local type of soil. Table A1. Sampling points coordinates, altitude as well as the local type of soil. Altitude Sampling Point Longitude Latitude Altitude (m) Soil Sampling Point Longitude Latitude Soil (m) Djidjikrut 1 39.109142 68.688389 2726 Regosol Djidjikrut 1 39.109142 68.688389 2726 Regosol Anzob tunnel adits 39.108853 68.687314 2703 Regosol Anzob tunnel adits 39.108853 68.687314 2703 Regosol Djidjikrut 2 39.126583 68.682944 2574 Regosol Djidjikrut 3 39.137944 68.663639 2444 Regosol Djidjikrut 2 39.126583 68.682944 2574 Regosol Djidjikrut 4 39.146806 68.651778 2398 Regosol Djidjikrut 3 39.137944 68.663639 2444 Regosol Djidjikrut 5 39.164528 68.641861 2318 Regosol Djidjikrut 4 39.146806 68.651778 2398 Regosol Djidjikrut 6 (Anzob 39.176333 68.627417 2252 Regosol Djidjikrut 5 39.164528 68.641861 2318 Regosol ore-mining combine) Djidjikrut 7 (Anzob Djidjikrut 6 (Anzob ore-mining combine) 39.176333 68.627417 2252 Regosol 39.199528 68.633278 1742 Regosol ore-mining combine) Djidjikrut 7 (Anzob ore-mining combine) 39.199528 68.633278 1742 Regosol Yagnob 1 39.217333 69.021111 2351 Regosol Yagnob 1 39.217333 69.021111 2351 Regosol Yagnob 2 39.216806 68.919333 2215 Regosol Yagnob 2 39.216806 68.919333 2215 Regosol Yagnob 3 39.172756 68.874414 2151 Regosol Yagnob 4 (before Ya Anzob gnob 3 39.172756 68.874414 2151 Regosol 39.162083 68.845222 2090 Regosol conﬂuence} Yagnob 4 (before Anzob confluence} 39.162083 68.845222 2090 Regosol Estuary of Anzob river Estuary of Anzob river to the Yagnob 39.150304 68.850006 2144 Regosol 39.150304 68.850006 2144 Regosol to the Yagnob Yagnob 5 (after Anzob confluence) 39.189667 68.758722 2070 Regosol Yagnob 5 (after Anzob 39.189667 68.758722 2070 Regosol Yagnob 6 39.192972 68.693472 1888 Regosol conﬂuence) Yagnob 6 39.192972 68.693472 1888 Regosol Yagnob 7 39.199972 68.640139 1739 Regosol Yagnob 7 39.199972 68.640139 1739 Regosol Yagnob 8 39.194278 68.598278 1706 Regosol Yagnob 8 39.194278 68.598278 1706 Regosol Yagnob 9 39.187472 68.543444 1657 Regosol Yagnob 9 39.187472 68.543444 1657 Regosol Saritag 1 39.028528 68.271278 2477 Regosol Saritag 1 39.028528 68.271278 2477 Regosol Saritag 2 Saritag 2 39.056417 3 68.346444 9.056417 68.346444 2194 2194 Regosol Regosol Konchoch 39.042167 68.332750 2361 Luvisol Kanchoch mine adit 39.039528 68.337889 2457 Luvisol Iskandardarya 1 39.101361 68.403583 2015 Regosol Iskandardarya 2 39.134028 68.453528 1820 Regosol Iskandardarya 3 (estuary of river) 39.186556 68.534944 1658 Regosol Fondarya 1 39.196389 68.536028 1644 Regosol Appl. Sci. 2022, 12, 2763 17 of 21 Table A1. Cont. Sampling Point Longitude Latitude Altitude (m) Soil Konchoch 39.042167 68.332750 2361 Luvisol Kanchoch mine adit 39.039528 68.337889 2457 Luvisol Iskandardarya 1 39.101361 68.403583 2015 Regosol Iskandardarya 2 39.134028 68.453528 1820 Regosol Iskandardarya 3 39.186556 68.534944 1658 Regosol (estuary of river) Fondarya 1 39.196389 68.536028 1644 Regosol Alovdin Lake 1 39.237642 68.254278 2780 Regosol Alovdin Lake 2 39.237472 68.261083 2780 Regosol Sarvoda 1 39.250194 68.268889 2620 Regosol Sarvoda 2 39.262944 68.310917 2488 Cambisol Sarvoda 3 39.246278 68.355750 2358 Cambisol Sarvoda 4 39.252111 68.405083 2166 Gleysol Sarvoda 5 39.226611 68.441028 1958 Gleisol Sarvoda 6 39.223194 68.484611 1808 Gleisol Sarvoda 7—estuary of 39.219889 68.527639 1660 Regosol river Fondarya 2 39.225167 68.530250 1626 Regosol Pete 1 (right tributary to 39.248639 68.561778 1895 Gleisol Fondarya) Pete 2 (right tributary to 39.249361 68.549889 1710 Gleisol Fondarya) Fondarya 3 39.258806 68.544000 1589 Regosol Kumargi Bolo 1 39.276861 68.573056 2029 Regosol Kumargi Bolo 2 39.275444 68.547583 1690 Regosol Chore 1—upper of river 39.313639 68.479694 2148 Regosol Chore 2—adit 39.308944 68.506194 1863 Regosol Chore 3—adit 39.308639 68.514056 1753 Regosol Chore 4—adit 39.308222 68.528694 1577 Regosol Chore 5—estuary of 39.306083 68.532917 1580 Regosol river Fondarya 4 39.305528 68.533861 1580 Cambisol Fondarya 5 39.344750 68.554333 1466 Cambisol Kumargi poyon 1 39.325944 68.628389 3629 Gleysol Kumargi poyon 2 39.363167 68.602694 1782 Gleysol Kumargi poyon 3 39.363967 68.561083 1434 Gleysol Fondarya 6 39.380528 68.549556 1389 Cambisol Zarafshon 1 39.452667 70.426100 2732 Regosol Zarafshon 2 (Dihisor) 39.426194 70.307583 2612 Regosol Zarafshon 3 (Dihisor) 39.444472 70.189750 2517 Regosol Zarafshon 4 (Paldorak) 39.457583 70.076194 2423 Regosol Zarafshon 5 (Paldorak) 39.426417 69.963444 2330 Regosol Zarafshon 6 (Sabak) 39.447639 69.841194 2272 Regosol Zarafshon 7 39.453167 69.723861 2267 Regosol (Madrushkat) Rovut– tributary to 39.449194 69.676306 2242 Regosol Zarafshon Zarafshon 8 39.440358 69.601324 2158 Regosol (Madrushkat) Madrushkat– tributary 39.446944 69.563472 2123 Regosol to Zarafshon Appl. Sci. 2022, 12, 2763 18 of 21 Table A1. Cont. Sampling Point Longitude Latitude Altitude (m) Soil Tributary 2—to 39.439889 69.542361 2075 Regosol Zarafshon (Isizi poyon) Zarafshon 9 Isizi poyon) 39.431222 69.483639 1999 Regosol Tributary 3—to 39.415750 69.418694 1985 Regosol Zarafshon (Isizi poyon) Zarafshon 10 (Isizi 39.413306 69.376833 1927 Regosol poyon) Zarafshon 11 (Pastigov) 39.413833 69.269194 1919 Regosol Kallakhona–tributary to 39.418194 69.264861 1913 Regosol Zarafshon Oburdon (Pastigov) 39.425611 69.167250 1875 Regosol Zarafshon 12 (Pastigov) 39.417056 69.156833 1820 Regosol Zarafshon 13 39.401222 69.060500 1742 Regosol (Shamtuch) Zarafshon 14 (Veshab) 39.402833 68.954028 1660 Regosol Zarafshon 15 (Shavadki 39.391472 68.853306 1619 Regosol poyon) Zarafshon 16 (Rarz) 39.380639 68.773361 1508 Regosol Zarafshon 17 (Fatmev) 39.385861 68.673861 1462 Regosol Zarafshon 18 39.387250 68.570250 1405 Regosol (Sangiston) Shahriston 1, tributary 39.520806 68.553389 2728 Regosol right site of tunnel Shahriston 2, tributary 39.519972 68.554889 2744 Regosol left site of tunnel Shahriston 3–estuary 39.440583 68.541389 1682 Luvisol Zarafshon 19 39.419455 68.509311 1366 Regosol Zarafshon 20 39.439194 68.441583 1306 Regosol Zarafshon 21 39.439194 68.441583 1284 Regosol Zarafshon 22 39.440806 68.273250 1226 Regosol Zarafshon 23 39.443472 68.087750 1206 Regosol Artuch 1 (Alpine camp) 39.274889 68.139167 2142 Luvisol Artuch 2 39.335278 68.087750 1573 Luvisol Artuch 3 39.397806 68.043250 1267 Regosol Zarafshon 24 39.471667 67.991833 1113 Gleysol Zarafshon 25 39.466472 67.887139 1072 Gleysol Obi Sara 1 39.379278 67.880028 1775 Regosol Obi Sara 2 39.415889 67.865639 1315 Regosol Obi Sara 3 39.468389 67.872833 1079 Regosol Zarafshon 26 39.497306 67.785056 1035 Gleysol Lake 1 39.113250 67.855250 2393 Regosol (Khazorchashma) Lake 2 (Marguzor) 39.140972 67.859528 2106 Regosol Lake 3 39.166083 67.838972 1888 Regosol Lake 4 39.197278 67.819333 1811 Regosol Lake 5 39.203564 67.810650 1718 Regosol Lake 6 39.210056 67.805028 1701 Regosol Lake 7 39.220306 67.800806 1610 Regosol Shing 1 39.240806 67.798028 1565 Regosol Shing 2 39.273667 67.802778 1382 Regosol Shing 3 industrial zone 39.306917 67.783778 1282 Regosol Mogiyon 1 39.112611 67.733639 2383 Gleysol Mogiyon 2 39.147750 67.737000 2144 Gleysol Mogiyon 3 39.215194 67.711944 1722 Gleysol Mogiyon 4 39.273722 67.688639 1474 Gleysol Mogiyon 5 39.315583 67.770167 1250 Luviysol Appl. Sci. 2022, 12, 2763 19 of 21 Table A1. Cont. Sampling Point Longitude Latitude Altitude (m) Soil Mogiyon 6 after junction with 39.339583 67.770306 1222 Regosol Shing river Mogiyon 7 39.378778 67.759472 1180 Regosol Mogiyon 8 39.419444 67.766083 1099 Regosol Mogiyon 9 39.456556 67.735889 1041 Regosol Mogiyon 10 39.495083 67.711861 994 Regosol Zarafshon 27 39.502889 67.678861 981 Regosol Zarafshon 28 39.496728 67.552247 934 Gleysol Zarafshon 29 39.529500 67.433860 883 Gleysol Table A2. The certiﬁed as well as experimentally determined mass fractions of the NIST 2709 CRM elements. Certiﬁed Measured Certiﬁed Measured Element Element (w%) (w%) (mg/kg) (mg/kg) Al 7.37 7.11 0.16 Sb 1.55 1.6 0.06 Ca 1.91 1.99 0.09 Ba 979 951 29 Fe 3.36 3.45 0.07 Cr 130 121 9.2 Mg 1.46 1.38 0.03 Co 12.8 13.6 0.3 K 2.11 2.15 0.06 Mn 529 546 19 Si 30.3 30.95 0.41 Sr 239 230 8 Na 1.22 1.26 0.03 V 110 121 11 Ti 0.34 0.3 0.01 Zr 195 201 50 Table A3. The matrix of Spearman’s correlation coefﬁcients of major elements (as oxides) in soils and sediments. All correlations signiﬁcant at p < 0.05 are represented in red (positive correlation) or blue (negative correlation) color. Sediments SiO TiO Al O FeO MnO MgO CaO K O 2 2 2 3 2 2 TiO 0.251 Al O 0.302 0.840 2 3 FeO 0.340 0.758 0.819 MnO 0.018 0.621 0.639 0.510 MgO 0.804 0.381 0.357 0.382 0.013 CaO 0.752 0.195 0.184 0.153 0.191 0.577 K O 0.155 0.612 0.627 0.728 0.392 0.268 0.260 Na O 0.204 0.419 0.410 0.276 0.313 0.066 0.435 0.262 Soils SiO TiO Al O FeO MnO MgO CaO K O 2 2 2 3 2 2 TiO 0.081 Al O 0.119 0.645 2 3 FeO 0.291 0.445 0.348 MnO 0.009 0.442 0.456 0.300 MgO 0.671 0.062 0.035 0.153 0.022 CaO 0.668 0.436 0.527 0.123 0.356 0.463 K O 0.213 0.543 0.626 0.459 0.255 0.108 0.276 Na O 0.081 0.536 0.403 0.422 0.378 0.011 0.268 0.431 References 1. Prokhorov, A.M. Zarafshon (river in Central Asia). 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Applied Sciences – Multidisciplinary Digital Publishing Institute

Published: Mar 8, 2022

Keywords: Zarafshon; Tajikistan; sediments; soils; INAA; felsic material; REE

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On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan

On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan

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On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan

On the Geochemistry of Major and Trace Elements Distribution in Sediments and Soils of Zarafshon River Valley, Western Tajikistan

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