BISAC SCI019000 Earth Sciences / General
Paleomagnetic studies of the early Carboniferous strata of Tuva have been carried out. As a result of the component analysis, post-folding secondary and pre-folding, probably close to the primary components of magnetization, were identified in them. Coordinates of the paleomagnetic pole for the Lower Carboniferous of Tuva: Φ = 53.8∘N, Λ = 141.7∘ E, A95 = 9.6∘. The lower Carboniferous strata of Tuva were formed at high latitudes: 51–70.5∘N. The Tuva block as a whole did not experience significant rotations relative to Siberia in the Phanerozoic. Nevertheless, in the Late Devonian in the territory of Tuva, shear deformations and rotations of rocks in the horizontal plane took place.
Magnetization, paleolatitude, tectonic alignment, declination, inclination
Early Carboniferous geological strata of Tuva are an element of the Central Asian Fold Belt (CAFB). The CAFB structures from the south build up the Siberian platform. The folded base of the CAFB in Tuva was formed as a result of accretion processes in the late Cambrian-early Or- dovician. As a result of the tectonic implacement of Precambrian and Cambrian terranes, the so- called “Caledonides” CAFB were formed. Cale- donian structures are widespread in Tuva, Mon- golia, Kazakhstan and other regions [Berzin and Kungurtsev, 1996; Belichenko et al., 1994; Do- bretsov et al., 2003; Gordienko et al., 2007; Kazan- sky, 2002; Kovalenko, 2017a, 2017b;Kovalenko and Chernov, 2008; Kovalenko and Petrov, 2017; Ko- valenko et al., 1996, 2016; Metelkin, 2012, and oth- ers]. After the completion of accretion processes, a sedimentary, sometimes volcanogenic-sedimentary cover began to accumulate on the Caledonides of the CAFB, part of which are the Early Carbonifer- ous strata of Tuva. Despite the fact that active ac- cretionary processes in Tuva were completed after the formation of the Caledonids, numerous struc- tural unconformities are distinguished in the post- Caledonian cover. They indicate that the rocks also experienced deformations at this time. In a number of works [for example, Buslov, 2011], it is assumed that some deformations were associated with shears, which were active in various parts of the CAFB throughout the Paleozoic. Shear move- ments could lead to rotations of geological blocks in the plane of the layers. Such rotations can only be detected by the paleomagnetic method. Elu- cidation of the patterns of rotation of geological blocks in the geological structure of Tuva is one of the tasks of paleomagnetic studies, the results of which are presented in this article. Besides, since the early Carboniferous strata of Tuva accumulated on the structural extension of the Siberian continent, paleomagnetic data on them can be used to refine the apparent polar wander paths (APWP) of Siberia. APWP curves are key paleomagnetic characteristics necessary for calcu- lating the kinematic parameters of the Earth’s ge- ological blocks and global reconstruction. For the Siberian craton, several APWP curves were pro- posed at different times [Metelkin, 2012; Pavlov, tures with a sharp angular unconformity. The 2016; Pechersky and Didenko, 1995; Smethurst et Caledonides of Tuva unite the tectonically superal., 1998; Torsvik et al., 2012]. Each of the sub- posed Precambrian and Early Paleozoic strata of sequent curves substantially refines the previous the Tuva-Mongolian massif, fragments of the Ven- APWP curves. Nevertheless, even the most recent dian ophiolite association and Cambrian volcanoge- APWP curve for Siberia [Pavlov, 2016] for many nic-sedimentary complexes. The Tuva-Mongolian periods of the Phanerozoic is based on single pa- massif includes several tectonic blocks. The Naryn, leomagnetic determinations that require confirma- Morensky and Erzinsky blocks of sedimentary and tion. This article provides a new paleomagnetic igneous rocks, metamorphosed under the amphibodata that can be used to refine the Early Carbonif- lite-granulite conditions, are distinguished. The erous paleomagnetic pole of Siberia [Pavlov, 2016]. strata were deformed and metamorphosed in the Early Cambrian (536±6 Ma) and at the Cambrian- Ordovician boundary (497 ± 4, 489 ± 3 Ma) [Sal- The Main Geological Elements of Tuva nikova et al., 2001]. Fragments of ophiolites are represented by rocks of the lower part of the lay- Sedimentary and volcanogenic-sedimentary stra- ered complex and a dike complex. U-Pb age from ta of the Phanerozoic post-Caledonian cover of plagiogranites of the Agardag zone shows 570 ± Tuva overlap complexly deformed Caledonian struc- 1.7 Ma [Pfander and Kroner, 2004; Pfander et al., 2001]. Cambrian volcanic-sedimentary complexes stones. Middle and Upper Jurassic rocks unconwith olistostromes are considered as fragments of formably overlap more and more ancient rock comsuprasubduction systems [Berzin and Kungurtsev, plexes. The strata are composed of gray-colored 1996, etc.]. For limestones, there are early Cam- conglomerates, sandstones, siltstones, coals [Nedra, brian age determinations from archaeocyates and 1966; VSEGEI, 1963]. other species of flora and fauna [for example, Ne- The Ordovician, Silurian and Devonian strata dra, 1958, 1961, 1966; VSEGEI, 1963]. The period are deformed to varying degrees, crumpled into of accretionary Caledonian deformations is esti- folds and broken into blocks by faults. The Early mated by the age of the post-accretionary Kaachem Carboniferous strata in many areas lie flat (dip anbatholith - 485 Ma [Rudnev et al., 2015; Sugo- gles up to 10∘), in some - steep, and the Jurassic rakova, 2007] and proceeded in the Late Cambrian. strata are slightly deformed and mostly lie almost At this time, molasse strata formed in the lower horizontally. part of the post-Caledonian cover. In the mod- ern geological structure of Tuva, the strata of the post-Caledonian cover are mainly exposed within Objects of Paleomagnetic Research the Central Tuva trough (Figure 1). As a re- sult of geological survey, the strata of the Cen- tral Tuvinsky trough were stratigraphically dis- The Lower Carboniferous strata of the Censected in sufficient detail to geological stages. The tral Tuva trough were sampled for paleomagsequence of strata accumulation and their rela- netic analysis in central and southern Tuva (Figtionship has been reliably established. Sedimen- ure 1). In the south of Tuva, they are subditary strata were dated by assemblages of fossil vided from bottom to top into the Suglughem, flora and fauna. The Early Devonian volcanic Herbes, Baytag, Ekiotug, and Aktal formations strata in Tuva have not been dated by the ab- [Nedra, 1958, 1961]. The Suglukhem and Herbes solute geochronology methods, but dated by the formations were assigned to the Tournaisian stage U-Pb method in Khakassia [Vorontsov, 2015]. Mo- based on the finds of ichthyofauna (Strepsodus lasse sediments of the Ordovician age [Nedra, 1958, siberiacus, Rhizodopsis savenkovi Obr., Acanth- 1961] overlie the Caledonian structures with sharp odes sp., Ganolepis sp., Cycloptychius sp.) and unconformity. They are composed of members of plants (Pteridorachis f. modica Radcz). Baitag, red and gray conglomerates, gravelstones, sand- Ekiotug and Aktal formations - to the Visean stage stones, limestones and siltstones. The Silurian based on the finds of flora (Arctodendron Kidstrata overlie molasse strata without visible un- stoni, Pteridorachis f. modica Radcz., Protolepidoconformity. They are represented by sandstones, dendron megaphyllum Rodct., Angarodendron sp., siltstones, conglomerates, gravelstones and lime- A. tetragonum aff. Kidstonii Nath., Tomiodendron stones [Nedra, 1958, 1961]. Devonian rocks over- schmalhauseni (Chache) Radcz.). lap Silurian rocks with unconformity. The Lower Samples for paleomagnetic studies were taken Devonian strata include tuffs, tuff breccias, lava from two sections from thin-bedded sandstones, flows and subvolcanic bodies of basic, intermedi- siltstones, and mudstones of the Suglughem, Herate and felsic composition, limestones, sandstones, bes, and Baytag formations. A total of 57 samples siltstones, conglomerates and gravelstones [Nedra, were taken from the Lower Carboniferous strata. 1958, 1961, 1966; VSEGEI, 1963]. The Middle All samples in the sections were taken from diffeand Upper Devonian strata are composed of red- rent stratigraphic levels. colored sandstones, siltstones, conglomerates, grav- In the central part of Tuva (Figure 1), the Lower elstones, gray-colored marls, limestones and, less Carboniferous strata are divided into the Suglugoften, volcanic rocks of basic and intermediate com- khem, Kyzylgirin, Herbes formations of the Tourposition. Lower Carboniferous strata with uncon- naisian stage and the Baytag, Ekiottug, and Akformity overlie the Devonian and older complexes tal formations of the Visean stage [1966; VSEGEI, [Nedra, 1958, 1961, 1966; VSEGEI, 1963]. The 1963]. The strata are assigned to the first of strata include variegated and red-colored mem- them on the basis of fish (Strepsodus siberiacus bers of conglomerates, sandstones, siltstones, mud- Chab, Rhizodopsis Savencovi Obr., Acanthodes ex gr. Lopatni Rohon) and plants (Lepidodendron retained in magnetite-containing rocks up to the Schmalhauseni chachl., Knorria sp., Archaeopteris Curie point of magnetite, in red flowers - up to the sp., Pteridorhachis sp., Archaeopteris fissilis Schzal- Curie point of hematite. In samples with multicom- hauseni). The second - based on the fish (Rhab- ponent magnetization, the low-temperature com- doderma sp ind., Gonatodus, Elonichydae sp., Po- ponent (LT) is released in the temperature range laeniscoidei far) and plants (Pteridorachis f. mod- from 20 to 300-460∘C, and the high-temperature ica megaphyllum sp., Angarodendron, Bothroden- component of magnetization (HT) is released in dron, Arctodendron aff. Kidstoni Nath, Knorria the range from 300 to 580∘C, in the samples of red (Arctodendron), Knorria (Bothrodendron), Cor- rocks - up to 660∘C. The vectors of one-component doiles). magnetization are randomly distributed in all sec- Samples for paleomagnetic studies were taken tions. The genesis of this magnetization is un- from gray, purple, and red-colored thin-bedded known. The low-temperature components of the sandstones, siltstones, and mudstones mainly of the magnetization of the early Carboniferous rocks on Baytag, Ekiottug, and Aktal formations. A total the sphere are either grouped around the direc- of 389 samples were taken from eight sections. All tion of the Cenozoic magnetic field of the Earth samples in the sections were taken from different in the Tuva region, or distributed along a great stratigraphic levels. circle from the direction of the present-day field to the direction of high-temperature magnetization, Paleomagnetic Method or distributed randomly (Figure 3, Table 1). Ap- parently, this component of the magnetization is The treatment of paleomagnetic samples was of a viscous origin. The high-temperature compo- carried out in the paleomagnetic laboratory of nents of the magnetization of the lower Carbonifer- IGEM RAS. Two cubes with an edge of 1 or 2 cm ous rocks in different sections form groups of vec- were cut from each sample, depending on the value tors with different polarities. The scatter of di- of the magnetic susceptibility of the sample. Each rections in these groups depends on the number cube was subjected to thermal demagnetization in of samples with one-component chaotic magneti- the temperature range 20-680∘C. Thermal demag- zation from these sections. In sections 1, 6, 7, only netization was carried out in a heater protected one-component chaotic magnetization was identi- fied (Figure 1). In sections 2, 3, 4, one-component by permalloy screens. The earth’s magnetic field in the screens was compensated up to 10-15 nT. chaotic magnetization was detected in 40-60% of Most of the cubes were heated 12-16 times. The the samples. The directions of high-temperature measurement of the magnitude and direction of the magnetization in these sections are characterized magnetization of the samples was carried out on by a large scatter (Figure 3). These sections were a JR-6 magnetometer. A component analysis of excluded from the analysis. In sections 5, 8, 10, no magnetization was carried out on the Zijderveld one-component chaotic magnetization was found. diagrams [Kirschvink, 1980; Zijderveld, 1967]. The The directions of high-temperature components of average directions of the selected magnetization magnetization in these sections are characterized components were calculated for two cubes. The by acceptable accuracy (Figure 3). In section 9, components of the magnetization of the samples only 6 samples with one-component magnetization were analyzed on a sphere in geographic (GS) and were identified. They have been removed. The di- stratigraphic (SS) coordinate systems [Khramov et rections of the high-temperature components of the al., 1982; McFadden and Jones, 1981; Shipunov, magnetization in section 9 are well grouped (Fig- 1995], computer programs created by R. J. Enkin. ure 3). Thus, for further analysis, we used the high- temperature HT magnetization of sections 5, 8, 9, Results of Paleomagnetic Studies 10. Judging by the temperatures of destruction of the HT magnetization, its carriers, apparently, are magnetite and hematite. In ten sampled sections of early Carboniferous Fold test carried out by the method of compari- rocks of Tuva (Figure 1), either one or two, rarely son of mean directions [Khramov et al., 1982; Mc- three components of magnetization are distingui- Fadden and Jones, 1981; Shipunov, 1995] showed shed (Figure 2). One-component magnetization is that the average directions of the HT-components of the magnetization of the rocks of these sections are statistically equal in the SS and differ in the GS (Table 1). Ks/Kg = 5. The synfolding test also showed that the magnetization of these sections is prefolding. The maximum grouping of vectors of the HT-component is formed at 100% straighten- ing of the fold: 𝑁 = 4, 𝐷 = 66∘, 𝐼 = 76∘, 𝐾 = 155, 𝛼95 = 7.2∘. We also analyzed HT magnetization at the site level. The sites were combined from 4 to 8 samples from fragments of sections with similar at- titudes (Table 2). Kg/Ks = 13.7. The fold test per- formed by the method of comparison of means [Mc- Fadden and Jones, 1981; Shipunov, 1995] for six sites with the highest precision parameter of HT- magnetization (𝐾) - positive (Table 2). Thus, we believe that on the basis of fold tests, a pre-folding high-temperature magnetization of the early Car- boniferous sections is close to the primary. Discussion The coordinates of the Early Carboniferous pa- leomagnetic pole were calculated: Φ = 55∘ N, Λ = 138∘ E, A95 = 7∘ for all four sections, Φ = 55.5∘ N, Λ= 138.5∘ E, A95 = 7∘ over three sections. Ac- cording to the sites, the coordinates of the paleomagnetic pole: Φ = 53.8∘ N, Λ = 141.7∘ E, A95 = 9.6∘. An analysis of the inclinations of high-temperatu- re magnetization showed that the Early Carbonif- erous strata were formed at high latitudes: 55-62- 69∘N (minimum-average-maximum paleolatitude) in four sections, 54-62-70∘N in three sections. Comparison of our data with the Early Carbonif- erous poles of Siberia published in [Pavlov, 2016] showed that in the Early Carboniferous the studied geological strata were in the structure of Siberia: 𝐹 = 1.8∘ ±4.5∘ (4 sections), 𝐹 = 2.8∘ ±5.1∘ (3 sec- tions) (𝐹 is the difference between the expected and calculated inclinations of magnetization [Beck, 1980; Demarest, 1983]). The declination of the HT magnetization com- ponent of the Early Carboniferous rocks differs from the declination of the magnetization calcu- lated from the paleomagnetic poles for Siberia: 𝑅 = -80±18.7 (4 sections), 𝑅 = -79±20.2 (3 sec- tions) (𝑅 is the difference between the calculated and expected declinations of magnetization [Beck, 1980; Demarest, 1983]). How can these differences be explained? The investigated Early Carboniferous sections are sep- arated from each other by 300-400 km. The coincidence in the SS of the directions of the HT-components of the magnetization of the Early Carboniferous sections shows that after the Early Carboniferous in Tuva there were no local defor- mations that could lead to rotation of strata in the horizontal plane. This is also evidenced by the flat (from 0 to 20∘) occurrence of the majority of early Carbonaceous thicknesses in Tuva. That is, in this case, paleomagnetic data for the Early Carboniferous can be extended to a large geologi- cal block within Tuva, including at least the entire Tuva trough, and, most likely, most of Tuva (Tuva block). Could this block rotate relative to Siberia? Paleomagnetic poles calculated from Ordovician and undeformed horizontally lying Middle Devo- nian rocks of Tuva [Kovalenko and Lobanov, 2018a; Kovalenko et al., 2021], showed good convergence with the same age paleomagnetic poles of Siberia - for Tremadoc: 𝐹 = 3.5∘ ± 11.2∘, 𝑅 = 5.2∘ ± 11.5∘, for the Middle Devonian: 𝐹 = 10.6 ± 12.5, 𝑅 = 5.5 ± 17.5 [Beck, 1980; Demarest, 1983]. Hence it follows that the Tuva block as a whole has not rotated relative to Siberia since the Ordovician time. The Early Carboniferous paleomagnetic pole of Siberia was calculated from thirteen magmatic bodies of the Emyaksin Formation in the Vilyui River valley [Pavlov, 2016]. The primary magne- tization is justified by the presence of directions of different polarity. Possibly, there were local ro- tations of a small block in the Vilyui River basin in Siberia, from which the paleomagnetic pole was calculated [Pavlov, 2016]. In addition, it cannot be completely ruled out that the studied magmatic bodies of the Vilyui River valley are subvolcanic. Then the difference in declinations may be due to inaccuracy in determining their primary bedding elements. The difference in declinations can also be ex- plained if we assume that the early Carbonifer- ous strata of Tuva were remagnetized at a later time. Comparison with the late Carboniferous- Permian paleomagnetic poles of Siberia [Pavlov, 2016] showed that the differences in the declinations of the magnetization directions measured in Tuva and the “expected” Siberian directions of magnetization persist up to 250 Ma, up to the Permian-Triassic boundary. For the paleomagnetic pole 315 Ma - 𝑅 = -45 ± 17, 𝐹 = -13 ± 6, for the paleomagnetic pole 290 Ma - 𝑅 = -41 ± 17, 𝐹 = 0 ± 4.5. But the early Carboniferous pole of Tuva statistically coincides with the pole of 250 Ma of Siberia - 𝑅 = 0 ± 14, 𝐹 = -3.2 ± 3.9. If the assumption that the early Carboniferous rocks of Tuva were remagnetized 250 Ma ago at the Permian-Triassic boundary is correct, then the strata should have been remagnetized in an un- deformed state, and deformed after remagnetiza- tion. The assumption of the remagnetization of rocks is questionable, since the secondary compo- nents of the magnetization of reverse polarity close to the direction 4+5+6+7 (Table 1) are absent in the older strata of Tuva in all sections of different ages that we studied [Kovalenko, 2017a; Kovalenko and Lobanov, 2018a, 2018b]. In [Bachtadse et al., 2000], the secondary magnetization component of reverse polarity was revealed only in one section of the Late Silurian rocks of Tuva and, most likely, it is associated with the intrusion of the Middle Devo- nian intrusion several kilometers from the section. In addition, in the early Carboniferous sections of Tuva 5, 8, 9, 10 there are insignificant magneti- zation directions of direct polarity. The predomi- nantly reverse polarity of the magnetization in the Early Carboniferous sections of Tuva corresponds to the reverse polarity magnetization revealed in the Late Devonian-Early Carboniferous rocks of Siberia [Kravchinsky et al., 2002] and Mongolia [Bazhenov et al., 2016]. The primary magnetiza- tion of the early Carboniferous rocks of Tuva is also supported by the regular change in the direc- tions of magnetization from the Early Carbonifer- ous sequences with steep inclinations to the Late Devonian ones with gentle inclinations [Kovalenko et al., 2020]. It is important to note that the Middle Devonian rocks studied in [Kovalenko and Lobanov, 2018a] are characterized by a wide scatter in declination (Figure 4). One group of directions (D4N, D4R, D5) is close to the expected direction calculated from the Early-Middle Devonian pole of Siberia [Pavlov, 2016]. The second group of directions (D2, D3) sharply differs from it in declination. That is, strata with the directions of magnetization D2, D3 are rotated in the horizontal plane relative to Siberia clockwise at an angle of more than 90∘. The strata of both groups are territorially separated and separated by young faults [Kovalenko and Lobanov, 2018a]. Apparently, such rotations were associated with shear displacements. Since the Middle De- vonian strata are overlain by Early Carboniferous strata that are slightly deformed and not rotated in the horizontal plane, the time of shear deforma- tions can be estimated as Late Devonian. Conclusion 1.In the Lower Carboniferous strata of Tuva, post-folding secondary and pre-folding, prob- ably close to the primary components of mag- netization, are distinguished. 2.Coordinates of the paleomagnetic pole for the Lower Carboniferous of Tuva: Φ = 53.8∘N, Λ = 141.7∘E, A95 = 9.6∘. The Early Carboniferous strata of Tuva accumulated at high latitudes: 51-70.5∘N. 3.The Tuva block as a whole did not experience significant rotations relative to Siberia in the Phanerozoic. Nevertheless, in the Late Devo- nian in the territory of Tuva, shear deforma- tions and rotations of rocks in the horizontal plane took place. Acknowledgments. This work was carried out with the financial support of the Russian Foundation for Ba- sic Research, project No. 18-05-00022.
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