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Article

Provenance and Tectonic Implications of Sedimentary Rocks of the Paleozoic Chiron Basin, Eastern Transbaikalia, Russia, Based on Whole-Rock Geochemistry and Detrital Zircon U–Pb Age and Hf Isotopic Data

by
Ludmila I. Popeko
1,
Yulia N. Smirnova
2,
Victor A. Zaika
2,
Andrey A. Sorokin
2,* and
Sergey I. Dril
3
1
Kosygin Institute of Tectonics and Geophysics, Far Eastern Branch, Russian Academy of Sciences, 680000 Khabarovsk, Russia
2
Institute of Geology and Nature Management, Far Eastern Branch, Russian Academy of Sciences, 675000 Blagoveshchensk, Russia
3
Vinogradov Institute of Geochemistry, Siberian Branch, Russian Academy of Sciences, 664033 Irkutsk, Russia
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(3), 279; https://doi.org/10.3390/min10030279
Submission received: 20 January 2020 / Revised: 7 March 2020 / Accepted: 10 March 2020 / Published: 19 March 2020
(This article belongs to the Special Issue Mineralogical, Geochemical, and Isotope for Igneous Intrusions and Metamorphic Rocks of Siberian Craton)
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Abstract

:
The Chiron Basin extends along the southern periphery of the Siberian Craton and the western margin of the Mongol–Okhotsk Belt. Here, we present whole-rock geochemical data (major and trace elements and Sm–Nd isotopes) along with zircon U–Pb geochronology and Lu–Hf isotopic data from Paleozoic sedimentary rocks within the Chiron Basin to investigate their provenance and tectonic history. εNd(t) values of the siliciclastics rocks of the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations vary from −17.8 to −6.6, with corresponding two-stage Nd model ages (tNd(C)) ranging from 2.56 to 1.65 Ga. Detrital zircon grains from these rocks are predominantly Archean, Paleoproterozoic, and Carboniferous–Devonian in age. The data suggest that the southern flank of the Siberian Craton is the only viable source area for Archean and Paleoproterozoic zircon grains with Hf model ages (tHf(C)) of >2.20 Ga. The majority of zircon grains from sandstones from the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations are Devonian–Carboniferous in age. With respect to their Hf model ages, the zircon grains can be subdivided into two groups. The first group of Devonian–Carboniferous zircon grains is characterized by relatively old (mainly Paleoproterozoic) tHf(C) model ages of 2.25–1.70 Ga and the source was the southern margin of the Siberian Craton. The second group of Devonian–Carboniferous zircon grains is characterized by significantly younger (mainly Neoproterozoic) tHf(C) model ages of 1.35–0.36 Ga, which are consistent with a juvenile source, most likely eroded island arcs. Our data, show that sedimentary rocks of the Chiron Basin likely formed in a back-arc basin on the southern periphery of the Siberian Craton facing the Paleozoic Mongol–Okhotsk Ocean.

1. Introduction

The Mongol–Okhotsk Belt is one of the major structural elements of East Asia and probably represents the youngest orogenic component within the collage of Central Asian orogenic belts ([1,2,3] and references therein). This NE–SW-oriented belt is located in northern Mongolia and Transbaikalia (Russia) and extends for over 3000 km from central Mongolia to Uda Bay in the Okhotsk Sea (Figure 1).
The Mongol–Okhotsk Belt is generally considered ([2,3,11,12,13] and references therein) to represent a remnant of the Mongol–Okhotsk Ocean, which closed owing to collision between the Siberian Craton and the Amuria Block (superterrane or microcontinent). However, many aspects of the evolution of this structure from ocean to suture zone remain unresolved.
Most controversial is the geodynamic framework of sedimentary formations and intrusive complexes within the Mongol–Okhotsk Belt, as well as the timing and nature of the accretion and collision. Constraints on the age and composition of sedimentary sequences within the Mongol–Okhotsk Belt and neighboring basins are required to better understand the evolution of the region. In this respect, U–Pb and Lu–Hf isotopic data from detrital zircon grains from a variety of different stratigraphic ages sedimentary sequences coupled with whole-rock Nd isotopic data are of crucial importance.
Recent geochronological studies have provided tighter constraints on the ages of Paleozoic sedimentary sequences in the western [14,15,16,17] and eastern [18,19,20,21] parts of the Mongol–Okhotsk Belt. In those studies, subduction zones of different age and polarity have been invoked to explain the evolution of the belt. Furthermore, detailed studies of Jurassic sedimentary rocks of the Mesozoic basins north [22,23,24] and south [25,26] of the Mongol–Okhotsk Belt have suggested that the Mongol–Okhotsk Ocean closed at the Early–Middle Jurassic boundary.
We performed whole-rock geochemical analyses together with U–Pb and Lu–Hf isotopic analyses of detrital zircon grains from late Paleozoic sedimentary rocks within the Chiron Basin to provide much-needed information regarding the evolution of the Mongol–Okhotsk Belt. The Chiron Basin is bordered by the southern edge of the Siberian Craton and the Transbaikal segment of the Mongol–Okhotsk Belt. Sedimentary formations within this basin carry important information regarding the geological events that occurred at the periphery of the Siberian Craton during the late Paleozoic associated with the evolution of the Mongol–Okhotsk Ocean.
Geological studies of Eastern Transbaikalia region have led to differing interpretations of the geodynamic nature of the Chiron Basin. Initially, Nagibina [27] identified this basin as a narrow synorogenic basin located at the north of the Mongol–Okhotsk Belt that was confined to the marginal fault zone. This interpretation was supported by Amantov [28], who termed the structures related to the Chiron Basin as “residual orogenic depressions” or “superimposed marginal basins”.
Consistent with the current conceptualization of the Mongol–Okhotsk Fold Belt, Parfenov et al. [2,29] interpreted the Chiron Group to represent accumulation of sediments in a forearc basin. However, they did not indicate a magmatic arc adjacent to this forearc basin. Ruzhentsev and Nekrasov [7] ascribed the formation of the Chiron Basin to instability caused by convergence of the Siberian Craton and Argun Continental Massif. A similar interpretation was proposed by Shivokhin et al. [9].

2. Geological Background

The Chiron Basin (Figure 1) is located in the northeastern Aga Zone [7,30] and occupies an area of >500 km2 on the left bank of the lower reaches of the Aga River and within the Chiron River basin. The late Paleozoic Chiron Basin is filled with about 3500–4000 m of unmetamorphosed shallow-marine siliciclastic rocks of the Chiron Group (Figure 2 and Figure 3). Extensive tectonic slices of the Chiron Group also occur to the west and north of the Chiron Basin, as well as in the southern spurs of the Mogoitui Range. Until the mid−1960s, the entire Chiron Group was assigned to the Permian [31]. Later, its age was reassigned to the late Visean to early Permian based on fossil content [32]. The Chiron Group lies unconformably upon metamorphic schists [33] known formerly as the Onon Formation, which was originally assigned a Silurian age by Tolukhonov [31]. However, Amantov [28] and Anashkina et al. [30] suggested a Proterozoic age for these rocks. Recently, metamorphic rocks of the Onon Formation have been regarded as late Paleozoic (middle Paleozoic, according to the Russian stratigraphic nomenclature) and are now termed the Aga–Borshchovochnyi metamorphic complex [9,34] (Figure 3).
The Chiron Group is a polycyclic stratigraphic sequence showing a gradual upward transition from coarse- to fine-grained siliciclastic rocks. Tutkhaltui, Khara–Shibir, Shazagaitui, and Zhipkhoshi formations [33] are assigned to late Visean through to the early Permian [32].
The Tutkhaltui Formation is separated by a sharp angular unconformity from the Aga–Borshchovochnyi metamorphic complex. From bottom to top, this formation consists of the following members [33]:
  • Conglomerates and sedimentary breccias interbedded with coarse-grained sandstones. Clastic material consists of angular fragments of the metamorphic schists and quartz. Pebbles of felsic volcanic rocks and of granite are rare. The clasts of the sandstones are angular. This member varies from a few meters to 40 m in thickness.
  • Massive medium- to fine-grained sandstones interbedded with calcareous sandstones and sandy siltstones 1–2 m thick, and lenses of bioclastic limestone. This member is 45 m thick.
  • Sandy siltstones gradually passing upwards into massive siltstone. This member is 43 m thick.
  • Massive medium- to coarse-grained sandstones interbedded with gray siltstones and sedimentary breccias similar in composition to Member (1). This member varies in thickness from 2 to 20 m.
  • Predominantly siltstones with rare thin interlayers of massive medium-grained sandstones. This member is 102 m thick.
The Tutkhaltui Formation contains numerous fossilized remains of bryozoans, brachiopods, bivalves, and crinoids [32,33]. Most brachiopod species occur widely in the Kuzbass, Mongolia, Verkhoyansk (Siberia), and Kolyma–Omolon regions of NE Russia [35]. In Mongolia [36] and the Verkhoyansk region [37], ammonoids of the genera Epicanites and Pachylyroceras also occur. These ammonoids are common in late Visean to Serpukhovian sedimentary rocks in Western Europe, the Urals, and North America [38]. On this basis, the Tutkhaltui Formation has been assigned a late Visean to Serpukhovian age.
The Khara–Shibir Formation conformably overlies the Tutkhaltui Formation and comprises two first-order cycles that have the same lithological composition and faunal assemblages. The first-order cycles are considered as Lower and Upper subformations. From bottom to top, the Lower Subformation consists of the following members [33]:
  • A conglomerate member, including two second-order cycles, consisting of medium and fine pebble conglomerates grading upwards into coarse-grained sandstones. Well-rounded pebbles are felsic volcanic rocks (90%), granites (6%), quartzites (2%), sandstones or siltstones (2%). Sandstones contain angular and poorly sorted clasts. Individual cycles vary in thickness from 20 to 40 m.
  • Alternating massive siltstones and sandy siltstones with flow structures, with gradual transitions between units. This member is 120 m thick.
  • Alternating fine- to medium-grained massive and bedded sandstones and massive siltstones. Individual layers are 5–20 m thick, the overall thickness of this member is up to 250 m thick.
The Upper Subformation comprises the following members [33]:
  • Predominantly coarse-grained rocks including second-order cycles consisting (from bottom to top) of medium and fine pebble conglomerates, coarse- to medium-grained sandstones, and sandy siltstones grading into massive siltstones. Individual cycles vary in thickness from 20 to 30 m. Pebbles are dominated by felsic volcanic rocks, together with granites, quartz, quartzites, and gray siltstones. This member is 90 m thick.
  • Alternating beds of massive medium- to fine-grained sandstones, massive siltstones, and sandy siltstones with gradual transitions between units. Siltstone and sandy siltstone layers are 6–27 m thick and sandstones 1–12 m thick. Single pebbles of felsic volcanic rocks are present at the base of sandy siltstone layers. This member is about 200 m thick.
  • Mainly siltstones with intercalations of sandstones as thick as 0.2–3 m irregularly distributed within vertical thickness. The member is up to 280 m thick.
  • Alternating beds of massive coarse-grained sandstones, medium-grained sandstones, and sandy siltstones with flow texture. Layers vary in thickness from 14 to 40 m. Coarse-grained sandstones contain flattened fragments of siltstone 2–3 cm in size. The member is 190 m thick.
The Khara–Shibir Formation is characterized by an extensive assemblage of bryozoans, brachiopods, bivalves, and crinoids [32,33]. Brachiopods in the Khara–Shibir Formation and the underlying Tutkhaltui Formation share a large number of common species. The Khara–Shibir brachiopods are most similar to brachiopods from the Waagenoconcha gigantea Zone (upper part of the Magarsky super-stratohorizon) in the Kolyma–Omolon region [39] and the Sajakella formosa Zone (upper part of the Khatynakh stratohorizon) in the South Verkhoyansk region [35]. Considering the stratigraphic position of the aforementioned analogs of the Khara–Shibir Formation, which overlie layers containing late Visean–Serpukhovian ammonoids and lie below sediments containing late Bashkirian ammonoids, an early Bashkirian age for the Khara–Shibir Formation is implied.
  • The Shazagaitui Formation conformably overlies the Khara–Shibir Formation. From bottom to top, the succession consists of the following members [33]:
  • A conglomerate member comprising second-order cycles consisting of coarse-, medium-, and fine-grained pebble conglomerates grading upward into sandstones and siltstones. Individual cycles vary in thickness from 10 to 70 m. Pebbles comprise felsic volcanic rocks (55%), granites (23%), quartzites (10%), granite porphyries (9%), sandstones and siltstones (2%), and quartz (1%).
  • Alternating beds of massive siltstones and sandy siltstones with flow structures, with gradual transitions between units. Interbeds of fine- to medium-grained sandstones 0.5−2 m in thickness with distinct planar boundaries show no regular pattern. This member is >500 m thick.
  • Massive coarse-grained sandstones passing upward into medium- and fine-grained rocks with rare interbeds of dark-gray massive siltstones 1–2 m thick. The thickness of this member exceeds 125 m.
  • Alternating beds of sandy siltstones with massive and flow structures and fine- to medium-grained sandstones, the latter in some places preserving cross-bedding. Intercalations of massive calcareous sandstones and sandy limestones also occur. The thickness of this member varies between 170 and 250 m.
The Shazagaitui Formation contains numerous remains of bryozoans, brachiopods, and crinoids [33]. Most brachiopod species are distributed throughout the Verkhoyansk region, (Siberia), and are associated with late Bashkirian ammonoids of the Braneroceras–Gastrioceras and Diabaloceras–Axinolobus zones [38,40]. On this basis, the Shazagaitui Formation has been assigned a late Bashkirian age [32]. Overall, the composition, texture, and structure of sedimentary rocks and benthic fauna suggest that the Shazagaitui Formation, as well as the underlying Tutkhaltui and Khara–Shibir formations, formed in a shallow- to moderately deep-marine environment close to the sedimentary source.
The Zhipkhoshi Formation in the central part of the Chiron Basin lies with a stratigraphic hiatus and visible conformity on the Shazagaitui Formation, and angular unconformity the Aga–Borshchovochnyi metamorphic complex in the marginal parts of the basin [33]. The Zhipkhoshi Formation is limited in extent, being restricted to the central part of the Chiron Basin, where the lower portions of the section are exposed. Stratigraphically higher horizons are truncated by a fault that bounds the Chiron Group to the northwest.
From the base upward, the Zhipkhoshi Formation consists of the following members: [33]:
  • Coarse-grained sandstones with intercalations of conglomerate. Pebble-to-boulder conglomerates comprising clasts composed mainly of rhyolite and quartzite and less commonly granitoid. This member varies irregularly in thickness between 90 to 170 m.
  • Siltstones containing plant detritus, fossil wood fragments, megaspores, and nodules formed around the remains of conularia and pelecipods. The thickness is about 300 m.
  • Medium- to fine-grained massive and bedded sandstones with scarce thin siltstone intercalations. The thickness of this member is 400 m.
  • Intercalated fine-grained massive and bedded sandstones and sandy siltstones. Sandstone horizons show cross-bedding and ripple marks. This member is 70 m thick.
On the basis of the assemblage of brachiopods and bryozoans, the Zhipkhoshi Formation is assigned a Sakmarian to early Artinskian age by analogy with the Verkhoyansk units, (Siberia), which, in addition to the brachiopods similar to the Zhipkhoshi brachiopods, contain ammonoids of the Uraloceras and Paragastrioceras genera [32,35]. The bivalve assemblage suggests a late Asselian to early Artinskian age for the Zhipkhoshi Formation [41]. Thus, the stratigraphic gap between the Shazagaitui and Zhipkhoshi formations spans the Moskovian, Kasimovian, and Gzhelian stages, and probably part of the Asselian stage, a total time span of about 18 Myr. Considering the stratigraphic unconformity between these formations, the inclusion of the Zhipkhoshi Formation within the Chiron Group is controversial [42,43].
The texture of sediments, in combination with the presence of plant detritus, megaspores, fossil wood, and benthic fauna, suggest that rocks of the Zhipkhoshi Formation accumulated in shallow-marine environments, whereas the angular clastic materials provide evidence for a close sedimentary source.
We investigated siliciclastic rocks of the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations, as well as schists of the Aga–Borshchovochnyi metamorphic complex, representing the basement rocks of the Chiron Basin. Sample locations are listed in Table 1 and are shown in Figure 2.

3. Analytical Methods

3.1. Major and Trace Element Analyses

Chemical compositions of siliciclastic rocks were studied using X-ray fluorescence analysis (XRF) (major elements, Zr) at the Institute of Geology and Nature Management, Far East Branch of the Russian Academy of Sciences, Blagoveshchensk, Russia, and inductively coupled plasma mass spectrometry (ICP-MS) (Cs, Ga, Rb, Sr, Ba, La, Ce, Pr, Nd, Sm, Eu, Gd, Tb, Dy, Ho, Er, Tm, Yb, Lu, Y, Nb, Hf, Ta, Th, U, Pb) at the Institute of Tectonics and Geophysics, Far East Branch of the Russian Academy of Sciences, Khabarovsk, Russia.
The powdered samples of sedimentary rocks were homogenized for XRF analysis by fusing with a mixture of Li metaborate and tetraborate in a muffle furnace at a temperature of 1050–1100 °C. Measurements were carried out on a 4S Pioneer X-ray spectrometer. Intensities of analytical lines were corrected for the background and for the effects of absorption and secondary fluorescence. For ICP-MS analyses, samples were decomposed with acid mixtures of HCl, HNO3, HF, and HClO4. Measurements were performed in a standard regime by Perkin Elmer/Sciex Elan 6100 DRC ICP-MS whose sensitivity over the whole mass scale was calibrated using standard reference solutions that contained all elements to be analyzed in the samples. The relative measurement error for major and minor elements was 3%–10%.

3.2. Sm–Nd Isotopic Analyses

Sm–Nd isotopic analyses were performed at the Collective Enjoyment Center of Isotope Geochemical Investigations, Vinogradov Institute of Geochemistry, Siberian Branch of Russian Academy of Sciences, Irkutsk, Russia. About 100 mg of the whole rock powder was dissolved in a mixture of HF, HNO3, and HClO4. A 149Sm–150Nd spike solution was added to all samples before dissolution. REE were separated on BioRad AGW50-X8 200–400 mesh resin using conventional cation exchange techniques. Sm and Nd were separated by extraction chromatography with LN-Spec (100–150 mesh) resin [44]. Total blanks during the measurement were 0.1–0.2 ng for Sm and 0.2–0.5 ng for Nd. Isotopic compositions of Sm and Nd were determined on a NEPTUNE Plus Multi-Collector ICP-MS in static mode. The precision (2σ) of Sm and Nd contents and 147Sm/144Nd ratios was ±0.4% and ±0.003% for 143Nd/144Nd ratios. 143Nd/144Nd ratios were normalized against 146Nd/144Nd = 0.7219. The results of the international standards were: 1) JNdi−1 (n = 40), 143Nd/144Nd = 0.512107 ± 4 (recommended value, 143Nd/144Nd = 0.512115 ± 7 [45]; 2) BCR−2 (n = 28), 143Nd/144Nd = 0.512630 ± 14; Nd = 28.77 ± 0.13 ppm; Sm = 6.52 ± 0.03 ppm; 3) AGV−2 (n = 8) – 143Nd/144Nd = 0.512769 ± 16; Nd = 30.3 ± 0.02 ppm; Sm = 5.42 ±0.03 ppm.
The εNd(t) values were calculated using the present-day values for a chondritic uniform reservoir (CHUR) 143Nd/144Nd = 0.512638 and 147Sm/144Nd = 0.1967 [46]. Whole-rock tNd(DM) mean crustal residence ages were calculated using the model of Goldstein and Jacobsen [47] according to which the Nd isotopic composition of the depleted mantle evolved linearly since 4.56 Ga ago and has a present-day εNd(0) value of +10 (143Nd/144Nd = 0.513151 and 147Sm/144Nd = 0.21365). To account for changes in the 147Sm/144Nd ratios due to fractionation of accessory minerals during granitoid melt crystallization, two-stage Nd model ages tNd(DM2-st) [48] were calculated from the mean crustal ratio 147Sm/144Nd = 0.12 [49].

3.3. Zircon U–Pb Dating

Zircons were isolated using conventional heavy liquid and magnetic techniques before handpicking under a binocular microscope at the Institute of Geology and Nature Management, Far East Branch of the Russian Academy of Sciences, Blagoveshchensk, Russia. Zircon grains were handpicked from concentrates and mounted in a 1” epoxy mount along with multiple fragments of zircon standards (FC, SL2, and R33). The mounts were imaged by BSE using a Hitachi S−3400N scanning electron microscope (SEM) equipped with a Gatan Chroma CL2 detector.
For geochronology, U–Th–Pb analyses of individual zircon grains were performed by laser ablation–inductively coupled plasma–mass spectrometry (LA–ICP–MS) at the Arizona LaserChron Center, Department of Geosciences, University of Arizona, Tucson, AZ, USA. For details of the analytical procedures, see [50]. The isotopic analyses involved the ablation of zircon using a Photon Machines Analyte G2 excimer laser coupled to a Thermo Element 2 single-collector–ICP–MS, using a drill rate of ~1 μm/s, resulting in a final ablation pit depth of ~15 μm. Grain selection and analysis sites were selected based on CL and BSE images with care taken to avoid inclusions and cracks. Calibration was performed using the FC zircon standard, with a well-established age of 1099.3 ± 0.3 Ma [51]. The Sri Lanka (SL2) and R33 [52] reference zircons were used as secondary standards for data quality control. Our 206Pb/238U and 207Pb/206Pb ages for SL2 zircon were 563.2 ± 4.8 Ma and 568 ± 16 Ma (2σ), respectively, which were in good agreement with the ID–TIMS ages reported by Gehrels et al. [53]. Our results yielded weighted mean 206Pb/238U and 207Pb/206Pb ages for the R33 zircon of 417 ± 7 Ma and 415 ± 8 Ma, respectively, which were consistent with the ages of Black et al. [52] and Mattinson [54].
Systematic errors were 0.9% for 206Pb/238U ratios and 0.8% for 206Pb/207Pb ratios (2σ). U concentrations and U/Th ratios were calibrated relative to the SL2 zircon standard and were accurate to ~20%. The concordia U–Pb ages were calculated using Isoplot v. 4.15 [55]. The following data were excluded from the final age calculations: data for which it was not possible to calculate a concordia age and 206Pb/238U and 207Pb/235U ratios with errors of >3%, as these exceeded the precision of the LA–ICP–MS method. The peak age was derived from the AgePick program developed by George Gehrels [56].

3.4. Hf-in-Zircon Isotopes

Hf isotope analyses were performed using a Nu Instruments high-resolution (HR)-ICP–MS and attached Photon Machines Analyte G2 Excimer laser at the Arizona LaserChron Center. Instrument settings were established first by analysis of 10 ppb solutions of JMC475 and a Spex Hf solution followed by analysis of 10 ppb solutions containing Spex Hf, Yb, and Lu. When all solutions yielded 176Hf/177Hf ratios of ~0.28216, instrument settings were considered optimized for laser ablation analyses and seven standard zircons (Mud Tank (MT), 91500, Temora (TEM), R33, FC52 (FC), Plesovice (PLES), and SL or (SL-F)) were analyzed. When precision and accuracy were considered acceptable, the unknowns were analyzed using the same acquisition parameters as for the standards.
Laser ablation analyses were conducted using a laser beam diameter of 40 μm, with the ablation pits located on the U–Pb analysis pits. Each acquisition consisted of one 40-s integration on backgrounds (on peaks with no laser firing) followed by 60 one-second integrations with the laser firing. Analyses were performed using a typical laser fluence of ~5 J/cm2, a pulse rate of 7 Hz, and an ablation rate of ~0.8 μm/s. Each standard was analyzed once for every ~20 unknowns. For details of the analytical procedures, see [50].
The 176Hf/177Hf ratio at the time of crystallization is calculated from measurement of present-day 176Hf/177Hf and 176Lu/177Hf ratios, using the decay constant of 176Lu (λ = 1.867 × 10−11) from Scherer et al. [57] and Söderlund et al. [58]. Calculation of εHf(t) values is based on the chondritic ratios of 176Hf/177Hf (0.282785) and 176Lu/177Hf (0.0336) given by Bouvier et al. [59]. The mantle model age tHf(DM) was calculated using the measured 176Lu/177Hf ratio of the zircon, although this only provides a minimum age for the source material of magma from which the zircon crystallized. Therefore, we also calculated the crustal model age tHf(C), which assumes that the parental magma of the zircons was produced from average continental crust. 176Lu/177Hf ratios for average continental crust vary significantly from ~0.001 to 0.023 [60]. Vervoort and Patchett [60], Amelin and Davis [61] proposed a 176Lu/177Hf ratio of 0.0093 for the average continental crust, while Griffin et al. [62] recommended a value of 0.015. However, we considered a value of 0.093 to more realistically reflect the 176Lu/177Hf ratio of average continental crust, because in some cases the use of the higher ratio results in Hf crustal model ages that are unrealistically higher than the corresponding whole-rock Nd model ages [63,64,65]. The tHf(C) values calculated for 176Lu/177Hf ratio of 0.015 are given in Supplementary Materials Table S3 for comparison. The depleted mantle line was defined by present-day 176Hf/177Hf = 0.28325 and 176Lu/177Hf = 0.0384 [62].

4. Results

4.1. Major and Trace Element Geochemistry

Chemical composition of siliciclastic rocks of the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations are given in Supplementary Materials Table S1.
On a log(SiO2/Al2O3) versus log(Na2O/K2O) classification diagram, [66], the siliciclastic rocks from all formations plot as greywacke (Figure 4a). On a log(SiO2/Al2O3) versus log(Fe2O3/K2O) classification diagram, [67], the samples plot mostly as arkose and wacke, and rarely as litharenite (Figure 4b). All samples had low values of the Chemical Index of Alteration (CIA = 53−40), Chemical Index of Weathering (CIW = 60−42)), and high values for the Weathering Index of Parker (WIP = 97−60) and Silica-Titania Index (STI = 90−84) (Supplementary Materials Table S1), indicating that rocks in the source area recorded low degrees of weathering. A CIA versus WIP diagram [68] shows that the siliciclastic rocks plot as fresh rocks (Figure 4c).
Sandstones and siltstones from the Khara–Shibir (Figure 5a, Table S1) and Shazagaitui (Figure 5b, Table S1) formations have low to moderate REE contents (ΣREE = 42–229 ppm) and moderate to weak negative Eu anomalies (Eu/Eu* = 0.59–0.94) compared with siliciclastic rocks of the Zhipkhoshi Formation (ΣREE = 67–187 ppm, Eu/Eu* = 0.64–0.95) (Figure 5c, Table S1). Trace-element variation diagrams for siliciclastic rocks from the Khara–Shibir (Figure 6a, Table S1) and Shazagaitui (Figure 6b, Table S1) formations show depletions in U, Th, Pb, Nb, Ta, REE, Sc, Co, and V relative to upper continental crust. Sandstones and siltstones of the Zhipkhoshi Formation have higher concentrations of these elements (Figure 6c, Table S1).

4.2. Zircon U–Pb Dating

4.2.1. Sample Y−99: Greenschist of the Aga–Borshchovochnyi Metamorphic Complex

Out of 122 detrital zircon grains from sample Y−99, 112 grains yielded concordant ages ranging mainly from c. 2900 to 492 Ma (Figure 7a, Table S2). The major age peaks on probability diagrams are at c. 2512, 1888, 888, 807, 583, 514 Ma, and rare zircon grains have concordant Paleoproterozoic and Archean ages. The youngest concordant zircon age is 492 ± 6 Ma (Late Cambrian).

4.2.2. Sample Y−98: Sandstone of the Khara–Shibir Formation

A total of 114 concordant ages were obtained from 130 detrital zircon grains in sample Y−98 (Figure 7b, Table S2). The estimated ages were mostly Carboniferous and Devonian (age peaks at c. 353 and 382 Ma). A single grain had a concordant zircon age of c. 429 Ma (Silurian), and another had a concordant age of c. 506 Ma (Cambrian). The youngest concordant zircon age was 330 ± 4 Ma (Early Carboniferous).

4.2.3. Sample Y−97: Sandstone of the Shazagaitui Formation

Analyses of 116 detrital zircon grains from sample Y−97 yielded 82 concordant ages. Most are Carboniferous (age peak at c. 334 Ma), Devonian (age peak at c. 379 Ma), and Paleoproterozoic to early Neoarchean (age peaks at c. 1.88, 2.41, and 2.50 Ga) (Figure 7c, Table S2).
Individual zircon grains had concordant Archean (c. 2.64 and 2.90 Ga), Paleoproterozoic (c. 2.13 and 2.07 Ga), Neoproterozoic (c. 879, 876, and 782, Ma), and Ordovician (c. 472 Ma). The youngest concordant zircon age was 324 ± 4 Ma (Early Carboniferous).

4.2.4. Sample Y−94: Sandstone of the Zhipkhoshi Formation

Concordant ages, which varied mostly from 313 Ma to ~2780 Ma, were obtained from 105 detrital zircon grains out of 114 grains analyzed. Main age peaks were at c. 2025, 1928, 1862, 808, 500, 404, 379, and 328 Ma (Figure 7d, Table S2). In addition, rare grains had Neoproterozoic (c. 903, 897, and 861 Ma) and Archean (c. 2.78, 2.55, 2.52, 2.38, and 2.12 Ga) concordant ages. The youngest concordant zircon grain had an age of 313 ± 3 Ma (Late Carboniferous).

4.3. In Situ Zircon Lu–Hf Isotopic Analyses

The results of Lu–Hf isotope analysis are shown in Figure 8 and listed in Table S3. As follows from Section 4.2 and Figure 7 and Figure 8, major zircon age populations in the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations occurred in the Carboniferous–Devonian, Cambrian, Neoproterozoic, Paleoproterozoic, and Archean, and displayed a wide range of Hf model ages. The Paleoproterozoic and Archean zircons had Hf model ages (tHf(C)) ranging from 2.98 to 2.21 Ga. A group of Cambrian and Neoproterozoic zircons had younger Hf model ages (tHf(C)) of 1.53–1.00 Ga. A more complicated pattern was observed for the Hf isotopic composition of Carboniferous–Devonian zircon grains (Figure 8), which had tHf(C) values ranging from 1.88 to 0.46 Ga (Table S3). Similar Hf model ages values characterized zircon grains from the Aga–Borshchovochnyi metamorphic complex (Figure 8).

4.4. Whole-Rock Nd Isotopic Analyses

The results of Sm–Nd isotope analysis are presented in Figure 9 and Table 2. 147Sm/144Nd ratios of siliciclastic rocks from all formations range from 0.0982 to 0.1198. All samples were characterized by a wide spread in εNd(t) values from −17.8 to −6.6, with corresponding two-stage Nd model ages (tNd(C)) of 2.56–1.65 Ga. Sandstones of the Shazagaitui and Zhipkhoshi formations had both the lowest εNd(t) values (−17.8 to −7.3) and the oldest Nd model ages (tNd(C) = 2.56 to 1.70 Ga). Sandstones from the Khara–Shibir Formation had relatively high εNd(t) values of −8.2 to −6.6 and younger Nd model ages (tNd(C) = 1.78–1.65 Ga). Schists of the Aga–Borshchovochnyi metamorphic complex had similar isotopic characteristics to those of the Khara–Shibir Formation.

5. Discussion

5.1. Depositional Age of the Formations

The Aga–Borshchovochnyi metamorphic complex is tentatively assigned a late Paleozoic age (middle Paleozoic, according to the Russian stratigraphic nomenclature) [34], but the youngest concordant zircon age in this complex is 492 ± 6 Ma. We consider that if the Aga–Borshchovochnyi metamorphic schists were indeed late Paleozoic in age, then they would have contained Devonian and, possibly, early Carboniferous zircons, as is the case with the other formations. On this basis, a Cambrian age for the Aga–Borshchovochnyi metamorphic complex cannot be excluded. Alternatively, the complex contains rocks of different ages.
As shown in Section 2, the stratigraphic position of the Khara–Shibir Formation corresponds to the lower Bashkirian stage [32], with the youngest concordant zircon age being 330 ± 4 Ma, corresponding to the Visean–Serpukhovian boundary. On the basis of faunal data, the Shazagaitui Formation is assigned an upper Bashkirian stage [32]. The youngest concordant zircon age found in the sandstone of the Shazagaitui Formation is 324 ± 4 Ma, which essentially corresponds to the Mississippian–Pennsylvanian boundary and does not contradict its biostratigraphic age.
There is an inconsistency between the Sakmarian–early Artinskian [32] or late Asselian–early Artinskian ages [41] proposed for the Zhipkhoshi Formation, as determined from faunal data, and the youngest zircon concordant age of (313 ± 3 Ma). It looks somewhat odd considering that intense magmatism is recognized both in the Carboniferous and Permian in the region (see Section 5.2 therein).

5.2. Provenance

Given the major age populations and variability in isotopic compositions of zircon grains such as εHf(t) (from −17.8 to −6.6) from the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations and whole-rocks two-stage Hf model ages tHf(C) (from 2.56 to 1.65 Ga), we can assume that the sources of these zircons varied markedly. As structural analysis of the region attests [7,9,10,30,71,72,73,74,75], the oldest zircon grains in sandstones of the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations, which have Hf model ages (tHf(C)) of >2.20 Ga, could be derived from the southern edge of the Siberian Craton (Figure 1). Igneous and metamorphic complexes that represent fragments of the cratonic basement could be a source for these zircons. Suitable Archean rocks include c. 2.86 Ga tonalite gneiss [70], c. 2.78 Ga gneiss [76], c. 2.83 Ga granite [77], c. 2.62 and 2.52–2.40 Ga granite [78], c. 2.78 Ga metagabbro [79], and c. 2.64 Ga granite gneiss [80]. Moreover, amphibolite-facies metavolcanic and metasedimentary rocks containing zircon grains with ages of 2.90–2.70 Ga could be a source of the Archean zircons.
Paleoproterozoic granitoids are widespread around the periphery of the Siberian craton ([78,81,82,83,84,85,86,87,88,89,90,91,92,93,94,95] and references therein) and can be divided into eight groups by crystallization age: c. 2.52–2.40, 2.15–2.04, 2.06–2.00, 2.00–1.95, 1.95–1.90, 1.90–1.87, 1.87–1.84, and 1.76–1.71 Ga. Granulite-facies rocks of the Mogocha Formation, which were metamorphosed at 1873 ± 8 Ma [96], along with Paleoproterozoic (~1.87 Ga) gabbro-anorthosites [97], could also have been a source for Paleoproterozoic zircon grains within sedimentary rock assemblages of the Chiron Basin.
A small group of Neoproterozoic zircon grains with tHf(C) = 1.52–1.16 Ga (Figure 8, Table S3) could be derived from metamorphic rocks of the Ikat Terrane [10] or the Ikat–Bagdarin Zone [75], as well as island-arc complexes of the Kelyan Island Arc. In particular, plagiogranites (971 ± 14 Ma, [98]), gabbros (939 ± 11 Ma, [75]), and metabasalts (892 ± 16 Ma, [99,100]) have recently been discovered within this terrane. According to Gordienko et al. [99,100], the island-arc series includes calc-alkaline volcanic rocks with crystallization ages of 837 ± 11 and 789 ± 8 Ma [101].
Zircon grains with Cambrian ages are rare in sedimentary rocks of the Chiron Basin, and we report Hf isotope data from a single grain only (Figure 8, Table S3). This grain has a tHf(C) of 1.00 Ga and could be related to denudation of a differentiated andesite–dacite–rhyolite association assigned to the Caledonian stage of the Uda–Vitim island-arc system, which extends along the southern periphery of the Siberian Craton [100,102]. According to Gordienko [102], volcanic rocks have the following crystallization ages: 529 ± 3 Ma (plagio-rhyolites in the Eravna Area), 516 ± 5 Ma (quartz porphyry in the Eravna Area), 529 ± 3 and 534 ± 6 Ma (rhyolites in the Oldynda Area), and 530 ± 26 Ma (dacites in the Kydzhimit Area).
The majority of zircon grains from sandstones of the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations are Devonian–Carboniferous in age. In terms of Hf model ages, the zircon grains can be subdivided into two groups. The first group is characterized by relatively old (mainly Paleoproterozoic) model ages (tHf(C) = 2.25–1.7 Ga) (Figure 8, Table S3), the sources of which could be the southern fringe of the Siberian Craton, where granitoids of the Olekma Complex have an age of 358 ± 6 Ma [103]. In addition, granitoids of the Barguzin (or Vitimkan) Complex, which are dated at 330–310 Ma [104,105], could constitute a source of the early Carboniferous zircons. However, this is unlikely as the age of this complex is 297–279 Ma [106]. In addition, there is no certainty regarding the source of Late Devonian zircons. Conceivably, their sources could be intrusions of the Krestovsky and Kruchinin complexes [9], for which there are no reliable age data.
The second group of Devonian–Carboniferous zircons is characterized by significantly younger (mainly Neoproterozoic) model ages (tHf(C) = 1.35–0.36 Ga) (Figure 8, Table S3), suggesting derivation from a source with a significant juvenile component, likely to have been eroded island arcs. Considering the location of the Chiron Basin along the boundary between the southern margin of the Siberian Craton and the western segment of the Mongol–Okhotsk Fold Belt (Figure 1), the sources of such zircons could have been Paleozoic island arcs of the Mongol–Okhotsk Ocean, whose existence is inferred in most geodynamic models ([2,29,107] and references therein). Conceivably, a fragment of such an arc is the Zun–Shiveya Complex, which consists of rhyolites, rhyodacites, and granite porphyry, which have tentatively been ascribed as Late Devonian to early Carboniferous in age [9].
In conclusion, it should be noted that like zircon grains from the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations, zircon grains from the Aga–Borshchovochnyi metamorphic complex display a similar range of ages (with the exception of those with Devonian–Carboniferous ages) and have identical isotopic characteristics (Figure 8; Table 2, Table S3). This supports an interpretation in which Archean, Paleoproterozoic, Neoproterozoic, and Cambrian zircons of the Aga–Borshchovochnyi metamorphic complex and Khara–Shibir, Shazagaitui, and Zhipkhoshi formations were derived from the same source.
Sandstones of the Shazagaitui Formation have the oldest model tNd(C) ages of 2.65 Ga (Table 2), consistent with the observation that the highest number of Paleoproterozoic and Archean zircons occur in these rocks (Figure 7c). On this basis, we assume that source materials for these rocks must have been derived from the Siberian Craton. Sandstones from the Khara–Shibir and Zhipkhoshi formations have younger model ages (tNd(C) = 1.70–1.65 Ga) and contain fewer Paleoproterozoic and Archean zircons (Figure 7b,d). Considering the Hf isotope data, we suggest at least two sources, one within the Siberian Craton and another that does not represent reworked early Precambrian continental crust, such as the island arcs mentioned above.

5.3. Tectonic Environments of Sedimentation

For establishing compositions of source rocks, we used well-known discrimination diagrams based on the values and ratios of major and trace elements. Some of these diagrams are shown in Figure 10. Plots of data from siliciclastic rocks within the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations in Na2O–K2O–CaO (Figure 10a), (CaO + MgO)–(Na2O + K2O)–(SiO2/10) (Figure 10b), and F1 versus F2 diagrams (Figure 10c) indicate that the source areas were composed mainly of felsic–intermediate igneous rocks. However, plots of the data in Na2O–K2O–CaO (Figure 10a) and Zr/Sc versus Th/Sc) (Figure 10d) suggest a contribution of recycled material.
Additional diagrams were used to constrain the paleotectonic environments of sedimentation. In the bivariate diagrams (Fe2O3* + MgO) versus (Al2O3/SiO2), (Fe2O3* + MgO) versus (Al2O3/(CaO + Na2O), F3 versus F4, and SiO2 versus K2O/Na2O, data for siliciclastic rock samples of all formations suggest that they accumulated in island-arc and active continental-margin settings (Figure 11a−d). A similar conclusion can be drawn from the ternary diagrams (K2O + Na2O)–(TiO2 + Fe2O3 + MgO)–(SiO2/20) and Co–Zr/10–Th (Figure 11e,f). Thus, the geochemical features of the rocks indicate that the Khara–Shibir, Shazagaitui, and Zhipkhoshi formations were deposited in subduction-related settings.
On the whole, the geochemical characteristics of the siliciclastic rocks (Figure 11), including their wacke/greywacke composition (Figure 4a,b), weak degree of source weathering (Figure 4c), and the presence of interbedded conglomerate and gravelstone (see Section 2), are evidence that sedimentation proceeded in an active tectonic regime. Considering that the clastic sedimentary rocks were sourced from igneous and metamorphic rocks of the Siberian Craton on the one hand, and island arcs on the other, we believe that sedimentation occurred in a backarc-basin setting of the southern periphery of the Siberian Craton facing the Paleozoic Mongol–Okhotsk Ocean.

6. Conclusions

On the basis of our investigation of detrital zircon U–Pb and Hf isotope data and whole-rock Nd isotope data for sedimentary rocks of the Chiron Basin, we draw the following conclusions.
  • Geochemical characteristics of the siliciclastic rocks, as well as the presence of conglomerate and gravelstone interbeds, suggest that sedimentation occurred in an active tectonic regime.
  • The main source of sedimentary rocks of the Chiron Basin was igneous and metamorphic rocks from the southern periphery of the Siberian Craton. Devonian–Carboniferous zircon grains with relatively young (mainly Neoproterozoic) Hf model ages were derived from island arcs.
  • Combining the new data with regional geological data suggests that sedimentary rocks of the Chiron Basin likely formed in a back arc basin setting on the southern periphery of the Siberian Craton facing the Paleozoic Mongol–Okhotsk Ocean.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/10/3/279/s1, Table S1. Chemical composition of the sedimentary rocks of the Chiron Basin. Table S2. U–Th–Pb LA-ICP-MS data for zircons from metasedimentary rocks of the Chiron Basin. Table S3. Hf isotopic data for zircons from metasedimentary rocks of the Chiron Basin. References.

Author Contributions

Conceptualization, L.I.P., methodology, Y.N.S., V.A.Z., and S.I.D.; validation, Y.N.S., V.A.Z., A.A.S., and S.I.D., formal analysis, L.I.P., and A.A.S., investigation, L.I.P., Y.N.S., V.A.Z., and A.A.S., writing—review and editing, Y.N.S., V.A.Z., and A.A.S. All authors have read and agreed to the published version of the manuscript.

Funding

The reported study was funded by RFBR according to the research projects number 18−35−20004 and 18−05−00840.

Acknowledgments

The authors thank the staff of the analytical laboratories of the Institute of Geology and Nature Management, Far East Branch, Russian Academy of Sciences (O.G. Medvedeva, V.I. Rozhdestvina, E.S.Sapozhnik, E.V. Ushakova, and E.N. Voropayeva), Institute of Tectonics and Geophysics, Far East Branch, Russian Academy of Sciences (E.M. Golubeva, A.V. Shtareva, V.E. Zazulina), and Arizona LaserChronCenter of the University of Arizona (M. Pecha) for performing the analytical studies.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Tectonic scheme showing terranes in the northern segment of the Central Asian Orogenic Belt (compiled after [2,4,5,6,7,8,9,10]). Numbers in circles are structures (terranes, microcontinents, cratonic blocks): (1) Anga–Talanchan; (2) Baidarik; (3) Baikal–Muya; (4) Barguzin; (5) Bayan–Khongor; (6) Gargan; (7) Daribi; (8) Derbi; (9) Dzhida; (10) Dzabkhan; (11) Eravna; (12) Western Stanovoi; (13) Ikat; (14) Kan; (15) Kitoikin; (16) Ozernyi; (17) Onon; (18) Tarbagatai; (19) Tuva–Mongol; (20) Tunka; (21) Khamardaban–Olkhon; (22) Khamsarin; (23) Khangai; (24) Khentei; (25) Aga–Borshchovochnyi.
Figure 1. Tectonic scheme showing terranes in the northern segment of the Central Asian Orogenic Belt (compiled after [2,4,5,6,7,8,9,10]). Numbers in circles are structures (terranes, microcontinents, cratonic blocks): (1) Anga–Talanchan; (2) Baidarik; (3) Baikal–Muya; (4) Barguzin; (5) Bayan–Khongor; (6) Gargan; (7) Daribi; (8) Derbi; (9) Dzhida; (10) Dzabkhan; (11) Eravna; (12) Western Stanovoi; (13) Ikat; (14) Kan; (15) Kitoikin; (16) Ozernyi; (17) Onon; (18) Tarbagatai; (19) Tuva–Mongol; (20) Tunka; (21) Khamardaban–Olkhon; (22) Khamsarin; (23) Khangai; (24) Khentei; (25) Aga–Borshchovochnyi.
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Figure 2. Geological map of the western part of Chiron Basin (after [9,34] and our data).
Figure 2. Geological map of the western part of Chiron Basin (after [9,34] and our data).
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Figure 3. Simplified stratigraphic column for the sedimentary rocks of the Chiron Basin as well as underlying and overlapping formations (modified after [34]).
Figure 3. Simplified stratigraphic column for the sedimentary rocks of the Chiron Basin as well as underlying and overlapping formations (modified after [34]).
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Figure 4. Plots of log(SiO2/Al2O3) versus log(Na2O/K2O) after [66] (a), log(SiO2/Al2O3) versus log(Fe2O3/K2O) after [67] (b), and CIA versus WIP after [68] (c) for siliciclastic rocks of the Chiron Basin.
Figure 4. Plots of log(SiO2/Al2O3) versus log(Na2O/K2O) after [66] (a), log(SiO2/Al2O3) versus log(Fe2O3/K2O) after [67] (b), and CIA versus WIP after [68] (c) for siliciclastic rocks of the Chiron Basin.
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Figure 5. Chondrite-normalized REE patterns for siliciclastic rocks of the Chiron Basin. Chondrite normalizing values are from [69]; (a) Khara-Shibir Formation, (b) Shazagaitui Formation, (c) Zhipkhoshi Formation.
Figure 5. Chondrite-normalized REE patterns for siliciclastic rocks of the Chiron Basin. Chondrite normalizing values are from [69]; (a) Khara-Shibir Formation, (b) Shazagaitui Formation, (c) Zhipkhoshi Formation.
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Figure 6. Upper continental crust (UCC)-normalized trace element patterns for siliciclastic rocks of the Chiron Basin. UCC normalizing values are from [49]; (a) Khara-Shibir Formation, (b) Shazagaitui Formation, (c) Zhipkhoshi Formation.
Figure 6. Upper continental crust (UCC)-normalized trace element patterns for siliciclastic rocks of the Chiron Basin. UCC normalizing values are from [49]; (a) Khara-Shibir Formation, (b) Shazagaitui Formation, (c) Zhipkhoshi Formation.
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Figure 7. Probability diagrams showing age distributions of detrital zircons from Aga–Borshchovochnyi metamorphic complex and ciliciclastic rocks of the Chiron Basin. Data from Supplementary Table S2; (a) Aga-Borshchovochnyi metamorphic complex, (b) Khara-Shibir Formation, (c) Shazagaitui Formation, (d) Zhipkhoshi Formation.
Figure 7. Probability diagrams showing age distributions of detrital zircons from Aga–Borshchovochnyi metamorphic complex and ciliciclastic rocks of the Chiron Basin. Data from Supplementary Table S2; (a) Aga-Borshchovochnyi metamorphic complex, (b) Khara-Shibir Formation, (c) Shazagaitui Formation, (d) Zhipkhoshi Formation.
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Figure 8. Plots of crystallization age (Ma) versus εHf(t) for zircon grains from Aga–Borshchovochnyi metamorphic complex and siliciclastic rocks of the Chiron Basin. Data from Table S3.
Figure 8. Plots of crystallization age (Ma) versus εHf(t) for zircon grains from Aga–Borshchovochnyi metamorphic complex and siliciclastic rocks of the Chiron Basin. Data from Table S3.
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Figure 9. Plots of crystallization age (Ma) versus εNd(t) values for Aga–Borshchovochnyi metamorphic complex and siliciclastic rocks of the Chiron Basin (black lines, data from Table 2), in comparison with whole-rock compositions of the magmatic and metamorphic rocks of the Dzhugdzhur-Stanovoy Superterrane (grey field, data from [70]).
Figure 9. Plots of crystallization age (Ma) versus εNd(t) values for Aga–Borshchovochnyi metamorphic complex and siliciclastic rocks of the Chiron Basin (black lines, data from Table 2), in comparison with whole-rock compositions of the magmatic and metamorphic rocks of the Dzhugdzhur-Stanovoy Superterrane (grey field, data from [70]).
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Figure 10. Plots of Na2O–K2O–CaO after [108] (a), (CaO + MgO)–(Na2O + K2O)–(SiO2/10) after [49] (b), F1 versus F2 after [109] (c), and Zr/Sc versus Th/Sc after [110] (d) for siliciclastic rocks of the Chiron Basin. Fields for the various sources: A–andesites, D–dacites, GR–granodiorites, G–granites, R–recycled sediments.
Figure 10. Plots of Na2O–K2O–CaO after [108] (a), (CaO + MgO)–(Na2O + K2O)–(SiO2/10) after [49] (b), F1 versus F2 after [109] (c), and Zr/Sc versus Th/Sc after [110] (d) for siliciclastic rocks of the Chiron Basin. Fields for the various sources: A–andesites, D–dacites, GR–granodiorites, G–granites, R–recycled sediments.
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Figure 11. Tectonic discrimination plots of Fe2O3* + MgO versus Al2O3/SiO2 after [108] (a), Fe2O3* + MgO versus Al2O3/(CaO + Na2O) after [108] (b), F3 versus F4 after [109] (c), SiO2 versus K2O/Na2O after [109] (d), (K2O + Na2O)–(TiO2 + Fe2O3 + MgO)–(SiO2/20) after [111] (e), and Co–Zr/10–Th after [112] (f) for siliciclastic rocks of the Chiron Basin. Fields for the various tectonic settings: A—Oceanic island arc; B—Continental island arc; C—Active continental margin; D—Passive margin.
Figure 11. Tectonic discrimination plots of Fe2O3* + MgO versus Al2O3/SiO2 after [108] (a), Fe2O3* + MgO versus Al2O3/(CaO + Na2O) after [108] (b), F3 versus F4 after [109] (c), SiO2 versus K2O/Na2O after [109] (d), (K2O + Na2O)–(TiO2 + Fe2O3 + MgO)–(SiO2/20) after [111] (e), and Co–Zr/10–Th after [112] (f) for siliciclastic rocks of the Chiron Basin. Fields for the various tectonic settings: A—Oceanic island arc; B—Continental island arc; C—Active continental margin; D—Passive margin.
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Table
Table 1. Location and short description of samples.
Table 1. Location and short description of samples.
TimeSample No.GPS [x°x′x″]FormationPetrographic Descriptions
Chiron Basin
Early PermianY−94E, 115°19′15.3″
N, 51°31′32.3″		Zhipkhoshi FormationGray sandstone with feldspar (25%), quartz (20%), lithic fragments (8%), biotite, muscovite and chlorite (up to 1%) and with 0.10–0.18 mm grain size.
Late CarboniferousY−97E, 115°19′43.5″
N, 51°29′31.5″		Shazagaitui FormationYellowish-gray sandstone with quartz (40%), feldspar (30%), lithic fragments (15%), muscovite (10%) and with 0.10–0.30 mm grain size.
Late CarboniferousY−98E, 115°20′31.3″
N, 51°27′56.6″		Khara-Shibir FormationBrownish-yellow sandstone with feldspar (45%), quartz (20%), lithic fragments (20%), biotite (10%), small amount muscovite and chlorite (up to 1%) and with 0.10–0.50 mm grain size.
Late Paleozoic(?)Y−99E, 115°00′21.9″
N, 51°33′33.2″		Aga–Borshchovochnyi metamorphic complexGray greenschist with quartz (40%), feldspar (15%), lithic fragments (10%), biotite and muscovite (35%), small amount chlorite.
Table
Table 2. Whole-rock Sm-Nd isotopic compositions of the rocks of Chiron Basin.
Table 2. Whole-rock Sm-Nd isotopic compositions of the rocks of Chiron Basin.
SampleFormation/ComplexLithologyAge *, MaSm, ppmNd, ppm147Sm/144Nd143Nd/144NdErr **εNd(0)εNd(t)tNd(DM)tNd(C)
Y−92Khara–ShibirSandstone3302.0811.760.107650.51202516−12.0−8.216151783
Y−98Khara–ShibirSandstone3303.2419.930.098210.5120872−10.7−6.614021650
Y−96−3ShazagaituiSandstone3245.5831.930.106370.5118496−15.4−11.718442064
Y−97ShazagaituiSandstone3243.6121.790.100060.5115234−21.7−17.821752565
Y−93ZhipkhoshiSandstone3133.4921.750.097620.51181311−16.1−12.117522094
Y−94ZhipkhoshiSandstone3133.8521.940.106120.5120782−10.9−7.315181696
Y−99Aga-BorshchovochnyiGreenschist4923.6518.410.119820.5120162−12.1−7.318381841
Y−101Aga-BorshchovochnyiGreenschist4923.4021.010.098680.5119626−13.2−7.015731817
* Age of the youngest zircon grains. ** The errors (2σ) refer to the last digits.

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Popeko, L.I.; Smirnova, Y.N.; Zaika, V.A.; Sorokin, A.A.; Dril, S.I. Provenance and Tectonic Implications of Sedimentary Rocks of the Paleozoic Chiron Basin, Eastern Transbaikalia, Russia, Based on Whole-Rock Geochemistry and Detrital Zircon U–Pb Age and Hf Isotopic Data. Minerals 2020, 10, 279. https://doi.org/10.3390/min10030279

AMA Style

Popeko LI, Smirnova YN, Zaika VA, Sorokin AA, Dril SI. Provenance and Tectonic Implications of Sedimentary Rocks of the Paleozoic Chiron Basin, Eastern Transbaikalia, Russia, Based on Whole-Rock Geochemistry and Detrital Zircon U–Pb Age and Hf Isotopic Data. Minerals. 2020; 10(3):279. https://doi.org/10.3390/min10030279

Chicago/Turabian Style

Popeko, Ludmila I., Yulia N. Smirnova, Victor A. Zaika, Andrey A. Sorokin, and Sergey I. Dril. 2020. "Provenance and Tectonic Implications of Sedimentary Rocks of the Paleozoic Chiron Basin, Eastern Transbaikalia, Russia, Based on Whole-Rock Geochemistry and Detrital Zircon U–Pb Age and Hf Isotopic Data" Minerals 10, no. 3: 279. https://doi.org/10.3390/min10030279

APA Style

Popeko, L. I., Smirnova, Y. N., Zaika, V. A., Sorokin, A. A., & Dril, S. I. (2020). Provenance and Tectonic Implications of Sedimentary Rocks of the Paleozoic Chiron Basin, Eastern Transbaikalia, Russia, Based on Whole-Rock Geochemistry and Detrital Zircon U–Pb Age and Hf Isotopic Data. Minerals, 10(3), 279. https://doi.org/10.3390/min10030279

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