Age of Detritic Zircon and Composition of Cambrian-Ordovician Terrigenous-Carbonate Deposits in the Middle Reach of the Vilyui River (South of the Siberian Platform)

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The article presents result of lithological and mineralogical studies of Upper Cambrian and Lower Ordovician terrigenous-carbonate deposits within the Vilyui syneclise (the middle reaches of the Vilyui River, south of the Siberian platform). The composition of detritic zircon, garnet, tourmaline and chromium spinels were carried out in a sample from the Upper Cambrian Kholomolokh Formation and two samples from the Balyktakh Formation (Upper Cambrian–Lower Ordovician). Predominant sources of the detritic minerals were igneous and metamorphic rocks of the Archean–Paleoproterozoic basement of the Siberian platform: rocks of acidic and intermediate compositions, amphibolite-facies metasediments and granulite- and amphibolite-facies mafic-ultramafic complexes. Results of U-Th-Pb dating of zircon from the Kholomolokh and Balyktakh Formations of the middle reaches of the Vilyui River showed a noticeable difference in the demolition sources of terrigenous matter in the Late Cambrian and Ordovician times. The sample from the Upper Cambrian Kholomolokh Formation contains the youngest zircon with a predominance of Neoproterozoic ages (peak ages of 550 and 845 Ma) indicating the main source of demolition in the Late Cambrian time were Neoproterozoic terranes rocks which are widespread along the southern margin of the Siberian craton. The Early Ordovician rocks of the Balyktakh Formation contain the main zircon population (~70%) of the Paleoproterozoic (1880–1890 Ma) age. The Early Ordovician the most probable source of matter for the Vilyui syneclise was an uplift of the Archean-Paleoproterozoic basement in the Siberian platform central part that represented an eroded land during the Ordovician. The almost complete absence of younger zircon (~500–900 million years) in the Balyktakh deposits indicates a weak influence of the demolition source from the southeastern margin of the Siberian platform in the Ordovician time.

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A. Zaytsev

Geological Institute of the RAS

编辑信件的主要联系方式.
Email: a.v.zaitsev@bk.ru
俄罗斯联邦, Bldg. 1, 7, Pyzhevsky Lane, Moscow, 119017

K. Dokukina

Geological Institute of the RAS

Email: dokukina@mail.ru
俄罗斯联邦, Bldg. 1, 7, Pyzhevsky Lane, Moscow, 119017

I. Baksheev

Lomonosov Moscow State University

Email: ivan.baksheev@gmail.com
俄罗斯联邦, 1, Leninskie Gory, Moscow, 119991

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2. Fig. 1. Schematic map of Russia with the Siberian Platform boundary (a) and scheme of the middle course of the Vilyui River (b); simplified geological map of the studied area according to [Geological ..., 1960; Geological ..., 1964; Mikhailov and Tesakov, 1972; State ..., 2001] (c); outcrop of the middle part of the Balyktakh Formation on the left bank of the Vilyui River, 4-5 km upstream of the mouth of the Kuranakh River (d); summary stratigraphic column of the Lower Paleozoic sediments of the middle course of the Vilyui River (e). Vilyui, 4-5 km upstream of the mouth of the Kuranakh River (d); a summary stratigraphic column of the Lower Paleozoic sediments of the middle reaches of the Vilyui River (according to [Pokrovskii et al, 2022] with modifications) and their correlation with local (black line, according to [Pokrovsky et al., 2022]) and global (red line, according to [Geologic ..., 2020]) carbon-isotope curves (e). Positive (red) and negative (blue) global carbon-isotope excursions: Tremadocian (TSICE); Lower Middle Ordovician (Dapine) negative excursion (BDNICE); Middle Darryville (MDICE); Guttenbergian (GICE); Hirnantian (HICE). a, b - schemes: 1 - territory of the Siberian Platform, 2 - major rivers, 3 - roads: main (a) and local roads (b), 4 - settlements, 5 - boundaries of the studied area; c - geological map: 6 - Lower-Middle Cambrian, 7 - Upper Cambrian-Lower Ordovician, 8 - Lower Ordovician, 9 - Middle-Upper Ordovician, 10 - Upper Ordovician, Oyusut Formation, 11 - Lower Silurian, 12 - Upper Devonian, 13 - Upper Permian, 14 - Lower Jurassic, 15 - Quaternary sediments, 16 - Traps, 17 - discontinuities: authentic (a) and inferred (b), 18 - water areas (rivers), 19 - number and location of outcrop: VY01 - Kholomolokh Formation, VY02 - Balyktakh Formation; e - lithology: 20 - limestones, 21 - clayey limestones and marls, 22 - dolomitic limestones, 23 - alternation of dolomites, gypsum, limestones, marls and clays, 24 - dolomites, 25 - clays and siltstones, 26 - grey, reddish, clayey and sandy dolomites of the Kholomolokh Formation.

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3. Fig. 2. Microphotographs of sandy dolomites of the Kholomolokhskaya (a-c) and Balyktakhskaya (d-i) formations in parallel (a, b, d, e, g, h) and crossed (c, e, i) nicols of the polarisation microscope. Major mineral components: Dol - dolomite, Qtz - quartz, Kfs - potassium feldspar, Fe - iron oxides and hydroxides. Hereinafter mineral indices are given according to [Whitney, Evans, 2010].

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4. Fig. 3. Mineral composition of terrigenous sandy admixture of the studied samples on classification diagrams. a - ratio of quartz (Q), feldspars (F) and rock fragments (L) content, according to [Folk, 1980]): 1 - quartzarenites, 2 - subarcoses, 3 - sublitharenites, 4 - arkoses, 5 - litharcoses, 6 - feldspar litharenites, 7 - litharenites; b - ratio of the content of polycrystalline quartz, including quartzites (Qt), feldspars (F) and rock fragments (L), according to [Dickinson, Suczek, 1979; Dickinson et al, 1983]; c - ratio of monocrystalline quartz (Qm), feldspars (F) and fragments of reworked rocks (Lt), according to [Dickinson, Suczek, 1979; Dickinson et al., 1983]. 1-3 - origin of clastic material: 1 - continental block, 2 - volcanic arc, 3 - reworked orogen. Numbers (in the figure) indicate the types of drift sources: 1 - intracratonic, 2 - marginal seas, 3 - basement uplifts, 4 - mixed, 5 - quartz reworked, 6 - transitional reworked, 7 - lithic reworked.

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5. Fig. 4. Backscattered electron images of the main morphological types of garnet grains from the Kholomolokhskaya (a-d) and Balyktakhskaya (f-m) formations. a - garnet with a border of calcite and dolomite, b-d - fractured grains, f-i - medium-rolled non-zonal, weakly fractured grains, k-m - medium-good-rolled non-zonal or weakly-zoned rounded and elongated-rounded, non-fractured grains. Mineral inclusions: Dol - dolomite, Cal - calcite, Qtz - quartz, Ce, La - phosphates of Ce and La, Rt - rutile, Zrn - zircon, Kfs - potassium feldspar, Chl - chlorite. Black and white circles show the place of analysis on the scanning electron microscope (spot diameter 3 µm). The scale bar is 50 µm.

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6. Fig. 5. Triangular discriminative diagrams (mol %) for the studied garnet. (a) - Alm + Sps-Prp-Grs diagram [Mange, Morton, 2007]: A - granulite facies metapelites, charnokites and igneous rocks of medium acidic composition, B - amphibolite facies metapelites, Bi - igneous rocks of medium acidic composition, Ci - metabasites of high degrees of metamorphism, Cii - high-magnesian meta-ultramafics (metapyroxenites and metaperidotites), D - metasomatic rocks, metabasites of low degrees of metamorphism, granulites and calcareous-silicate rocks formed in granulite facies of ultrahigh temperature metamorphism. (b, c) - diagrams Alm-Prp-Grs (b) and Alm-Prp-Sps (c) ([Méres, 2008; Aubrecht et al., 2009], modified from [Knierzinger et al., 2019]). A - garnets from high and ultrahigh-pressure rocks, B - garnets from metamorphic rocks of eclogite and granulite facies, C - garnets from rocks of amphibolite facies. Transitional field C1 includes garnets from rocks metamorphosed at higher levels of amphibolite and granulite facies, while field C2 includes garnets from rocks of amphibolite facies, blue schists, skarns, serpentinites and igneous rocks. The numbered fields are: 1 - ultra-high-bar eclogites or garnet peridotites, 2 - high-bar eclogites and basic granulites, 3 - granulites of acidic and medium composition, 4 - gneisses formed in transitional conditions between granulite and amphibolite facies, 5 - amphibolites formed in transitional conditions between granulite and amphibolite facies, 6 - gneisses of amphibolite facies, 7 - amphibolites. (d) - distribution of selected garnet groups in samples. 1 - group I, 2 - group II, 3 - subgroup IIIa, 4 - subgroup IIIb, 5 - group IV.

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7. Fig. 6. Backscattered electron images of the main morphological types of tourmaline grains. a, b, d - rounded and elongated-rounded non-cracked or slightly cracked grains with concentric, rarely polygonal zoning from the Kholomolokhsky Formation (sample VY10/16); c - strongly cracked tourmaline grain from the Kholomolokhsky Formation; e, f - medium-cracked, non-zonal or with polygonal zonality tourmalines from the Balyktakh Formation (sample VY20/16); g-and - non-cracked rounded and elongate-rounded, spotty-zonal grains from the Balyktakh Formation (sample VY21/16). Mineral inclusions: Qtz - quartz, Rt - rutile, Zrn - zircon, Ap - apatite, Po - pyrrhotite. Black and white circles show the place of analysis on the scanning electron microscope (spot diameter 3 µm). The scale bar is 50 µm.

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8. Fig. 7. Triangular diagrams for tourmaline by parent rock type [by Henry, Guidotti, 1985]. (a) - Al-Al50Fe(tot)50-Al50Mg50 diagram: 1 - Li-rich granitoids, pegmatites and aplites, 2 - Li-poor granitoids, pegmatites and aplites, 3 - hydrothermally altered granitic rocks, 4 - metapelites and metapsammites, 5 - Al-poor metapelites and metapsamites, 6 - Fe3+-rich quartz-tourmaline rocks, calcisilicate rocks and metapelites, 7 - low-calcium ultramafics, 8 - metacarbonates and metapyroxenites. (b) - Ca-Fe-Mg diagram: 1 - Li-rich granitoids, pegmatites and aplites, 2 - Li-poor granitoids and associated pegmatites and aplites, 3 - Ca-rich metapelites, metapsammites and calcisilicate rocks, 4 - Ca-poor metapelites, metapsammites and quartz-tourmaline rocks, 5 - metacarbonates; 6 - meta-ultramafics.

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9. Fig. 8. Composition of clastic spinel in sample VY10/16 from the Kholomolokh Formation: triangular classification diagram Cr-Al-Fe3+ [Barnes and Roeder, 2001] (a); combined tectonic discrimination diagram #Mg-#Cr (#Mg = Mg / (Mg + Fe2+), #Cr = Cr / (Cr + Al) [Dick and Bullen, 1984; Hirose and Kawamoto, 1995; Pober and Faupl, 1988] (b). N-MORB - normal basalts of mid-ocean ridges.

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10. Fig. 9. U-Pb concordance diagrams showing the results of LA-ICP-MS analysis of zircon from rocks of the Kholomolokh (a) and Balyktakh (c, e) formations; histograms of 207Pb/206Pb ages and relative probabilities of zircon ages: Kholomolokh (b) and Balyktakh (d, e) formations. The histograms are constructed for concordant and near-concordant age values (D = -4-4%, see Table 3). On the scale of 207Pb/206Pb ages, grey lines indicate zircon occurrences of presumably metamorphic genesis.

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11. Fig. 10. Cathodoluminescence (CL) images of zircon from the Kholomolokhskaya (a-d) and Balyktakhskaya (e-m) formations. Zoning types: a, d, l - oscillatory, b, c, g, k - "spruce tree", h - "flame-shaped", e, i - "football", f, h, m - structureless. Dotted circles show the location of LA-ICP-MS analysis (30 μm spot diameter). The scale bar is 50 µm.

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12. Fig. 11. Diagram of Th/U ratio and 207Pb/206Pb ages for the studied zircon grains. Discrimination lines are drawn according to [Rubatto, 2002]. On the scale of 207Pb/206Pb ages, vertical grey fillings indicate zircon occurrences of presumably metamorphic genesis.

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13. Fig. 12. Schematic palaeogeographic maps of the Siberian Platform in the Late Cambrian (a) (according to [Sukhov, 2016] with modifications) and Early Ordovician, Late Jurassic (b) (according to [Kanygin et al., 2007] with modifications). 1 - Siberian platform boundary, 2 - major rivers, 3 - Lake Baikal, 4 - settlements; sedimentation settings and facies: 5 - low and high land; 6 - coastal sand facies, 7 - subaerial coastal settings (sebkha), 8 - dolomite stromatolite facies, 9 - shallow-marine, including tidal settings, 10 - western-shelf conditions, clay-carbonate facies, 11 - boundaries of facies zones; 12 - location of the studied area, 13 - assumed direction of terrigenous material drift: pink arrows - Upper Cambrian, Verkholensk time (according to [Gladkochub et al., 2022]), green arrows - Early Ordovician (according to [Glorie et al., 2014]), red arrows - the present work.

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