The Beginning of a Wilson Cycle in an Accretionary Orogen: The Mongol–Okhotsk Ocean Opened Assisted by a Devonian Mantle Plume

The opening of oceans within accretionary orogens is important for understanding the Wilson cycle. The Mongol–Okhotsk Ocean (MOO) began opening within the early Paleozoic accretionary collage of the Central Asian Orogenic Belt (CAOB), representing a world‐class example to constrain the geodynamic history of ocean opening in accretionary orogens, but the kinematics and mechanisms associated to this process are highly debated. We report on a newly‐discovered bimodal volcanic suite and associated volcanic‐sediments that comprise part of the Altay‐Sayan Rift System, which indicate a widespread Early Devonian extensional event within the CAOB. This extension regime is attributed to a Devonian mantle plume, which is thought to have impinged upon and weakened the lithosphere of the Early Paleozoic collage, and drove the opening of the MOO. Opening of the MOO suggests continent breakup in accretionary orogens tends to focus along intervening weak orogenic lithosphere between the rigid microcontinents.


Introduction
Precise constraints on continental breakup and consequent birth of new oceans play a key role in paleogeographic and tectonic models as they represent the initiation of the Wilson cycle (Brune et al., 2023;Wilson, 1966).Continental breakup has generally been attributed to either dynamic stresses imparted by uprising subcontinental mantle plumes (e.g., Cande & Stegman, 2011;Koptev et al., 2015), the tensional far-field stresses from slab rollback (e.g., Bercovici & Long, 2014;Dal Zilio et al., 2018), or the far-field effects of slab pull forces on the opposite margin of the same plate (e.g., following oceanic ridge subduction, Murphy et al., 2006;Wan et al., 2021).The mantle plume scenario is characterized by occurrence of large igneous provinces (LIPs), including flood basalts or silicic magmatic events (e.g., Bryan & Ernst, 2008;Torsvik et al., 2010).The slab rollback scenario is characterized by oceanward magmatic migration along the continental margin accompanied by back-arc extensions (Bercovici & Long, 2014;Nakakuki & Mura, 2013) that produced mafic magmas with geochemical variations between mid-ocean ridge basalt (MORB) and island-arc basalt (IAB) composition (e.g., Pearce & Stern, 2006).The far-field ridge subduction could give rise to a variety of rock assemblages, including MORB, A-type granites, adakites, Nb-enriched basalts and charnockites (e.g., Windley & Xiao, 2018).Thus, the magmatic record associated with the continent breakup can distinguish the dynamic driving forces of continent breakup and ocean opening.
A valuable field site where continental break-up can be studied for all its complexity and dynamics is the Central Asian Orogenic Belt (CAOB)-one of the largest accretionary collages in the world.The belt formed through multiple convergence and collisional events of various orogenic components from 1,000 to 250 Ma (e.g., Xiao et al., 2015).The peri-Siberian sector of the orogen mainly consists of microcontinents and Neoproterozoic-Cambrian subduction-accretionary complexes, which had been accreted to Siberia craton during Early Paleozoic related to the closure of the Pan-Rodinian Mirovoi Ocean (e.g., Buriánek et al., 2017;Wilhem et al., 2012;Zhu, Zhang, et al., 2023).The southern part of the CAOB predominantly comprises Mid to Late Paleozoic subduction-accretionary complex of the Paleo-Asian Ocean (e.g., Wilhem et al., 2012;Windley et al., 2007).The northern Early Paleozoic collage is crosscut by the young Mongol-Okhotsk orogenic belt, which preserves the evolution of the Mongol-Okhotsk Ocean (MOO) (Zorin, 1999; Figure 1).This Early Paleozoic orogenic domain is considered to be the site where the MOO opened during the Early-Middle Paleozoic (e.g., Domeier, 2018;Wilhem et al., 2012).These relationships provide the opportunity to investigate how accretionary orogens can be torn apart to form a new oceanic basin.The lack of precise constraints on kinematics, timing and mechanisms for the opening of the MOO has produced three contrasting models: (a) the MOO opened during Ediacaran-Cambrian times between the Siberian craton and the Tuva-Mongol massif (Sengör et al., 1993); (b) the MOO was a large embayment of the Paleo-Pacific, that opened in the Early Carboniferous-earliest Permian after the amalgamation of the Central Mongolian microcontinent and the Siberian Craton (e.g., Zorin, 1999); (c) the MOO opened by back-arc spreading during the latest Ordovician-Silurian within the Early Paleozoic collage of the CAOB (Bussien et al., 2011;Domeier, 2018).These models are speculative because the critical magmatic records of the initial MOO opening have not yet been found.
In this paper, we present new geochronological and geochemical data for Devonian bimodal magmatism and associated volcanic-sedimentary rocks in Northwest Mongolia.Integrated with the available records of the MOO, we propose a new tectono-magmatic scenario where the MOO opened in response to Devonian mantle plume   Zhou et al., 2018;Vorontsov et al., 2021).
upwelling, which weakened the crust of the Early Paleozoic accretionary orogen and resulted in continent breakup along weak orogenic lithosphere between the rigid microcontinents previously accreted to Siberia.

Geological Setting and Analytical Methods
The Mongol-Okhotsk orogenic belt extends more than 3,000 km from central Mongolia to the Uda Gulf in the Okhotsk Sea (Figure 1;Zorin, 1999;Bussien et al., 2011).Concentric horseshoe-shaped microcontinental ribbons and magmatic-arc belts, and U-shaped aeromagnetic pattern suggest the Mongol-Okhotsk orogenic belt has an arcuate geometry and likely represents an orocline that developed during the closure of the MOO between Siberian Craton and the Amur Block (Xiao et al., 2015;Zorin, 1999).The MOO began subducting during the Pennsylvanian (Zhu, Pastor-Galán, et al., 2023) and was consumed by subduction on both of its margins, southward under the Amur Block and northward under the Siberian Craton (Donskaya et al., 2013).The final closure of the MOO is estimated to have occurred between the Early-Middle Jurassic and Early Cretaceous, leading to the collision of the Siberian Craton with the Amur Block (e.g., Van der Voo et al., 2015;Yi & Meert, 2020).
We report in this paper a newly discovered bimodal volcanic suite found about 30 km north of the Ulgey city, Mongolia, around the hinge of the curved Mongol-Okhotsk orogenic belt (Figure 1; Figure S1 in Supporting Information S1).The Ulgey bimodal suite with a thickness of up to 400 m consists of alternating units of basaltic andesite-rhyolite association (Figure 2a).The suite is intercalated with the Early Devonian Tunget formation, which consists of conglomerate, tuff sandstone, felsic tuff, rhyolite, sandstone and limestone (Filippova et al., 1990).The Late-Devonian Sagsai formation consists of sandstone, conglomerate, mudstone, basalt, rhyolite and carbonate rock (Filippova et al., 1990).The presumed Silurian Mukhar formation consists of mudstone, sandstone, siltstone, basalt, rhyolite, tuff with interbedded conglomerate (Figure 2b), and is underlain by Cambrian to Early Ordovician Mongol Altai formation composed of metamorphosed and isoclinally folded flysch-like sequences (Badarch et al., 2002;Figure S1 in Supporting Information S1).
To obtain the age of the Ulgey bimodal suite and provenance information of the Cambrian-Devonian sedimentary rocks, two rhyolites from the Ulgey bimodal suite of the Tunget formation, three sandstones from the Mongol Altai formation, one siltstone from the Mukhar formation, and three sandstone/siltstone from the Sagsai formation (detailed sample locations shown in Figure S1 in Supporting Information S1) were selected for U-Pb zircon dating by laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS).Whole-rock major and trace-element compositions, and Nd isotope compositions for the Ulgey bimodal magmatic suite and basalts from the Mukhar formation were determined by X-ray fluorescence (XRF), ICP-MS and multi-collector (MC) ICP-MS, respectively.The detailed analytical procedures can be found in Supporting Information S1.

Zircon U-Pb Geochronology
The zircon U-Pb age results of 9 analyzed samples are given in Table S1 in Supporting Information S1 and Figures 2c and 2d.Zircons from two rhyolite samples 19MAT-169 and 19MAT-157 are euhedral to subhedral prisms that are 100-300 μm long.Most zircons show oscillatory zoning (Figure S2 in Supporting Information S1), a feature characteristic of igneous zircons.The measured U and Th concentrations vary from 54 to 3,283 ppm and from 28 to 6,078 ppm, respectively, with Th/U ratios between 0.41 and 1.20, also indicating an origin of igneous zircon (e.g., Rubatto, 2002).Fifteen analyses of sample 19MAT-169 yield a weighted mean 206 Pb/ 238 U age of 410 ± 4 Ma (MSWD = 0.89; Figure 2c), and 25 analyses of sample 19MAT-157 yield a weighted mean 206 Pb/ 238 U age of 415 ± 4 Ma (MSWD = 0.26; Figure 2c).Two analyses of sample 19MAT-169 yield older ages (ca.2,312 Ma and 541 Ma), which are interpreted to record inheritance.
Most of the detrital zircon grains from the siltstone/sandstone samples in this study are euhedral to subhedral with clear oscillatory zoning (Figure S2 in Supporting Information S1).Samples  from the Mongol Altai formation yield mainly Cambrian to Early Ordovician and Neoproterozoic ages with minor Paleo-Mesoproterozoic ages, and they have a prominent ∼512-510 Ma age peak (Figure 2d).Sample 19MAT-147 (siltstone) from the Mukhar formation mainly yields Cambrian to Early Ordovician, Early Devonian and Neoproterozoic ages with minor Silurian and Paleoproterozoic ages, and it has age peaks of ∼408 and ∼497 Ma (Figure 2d).Sample 19MAT-146 (siltstone), 19MAT-27 (sandstone) and 19MAT-09 (sandstone) from the Sagsai formation mainly yield Early-Middle Devonian and Cambrian to Early Ordovician ages, with minor Late Devonian-Early Carboniferous, Neoproterozoic and Paleoproterozoic ages, and age peaks of ∼386-390 Ma and ∼488-512 Ma (Figure 2d).
Four mafic and four felsic volcanic samples from the Ulgey bimodal suite, and three basalt samples from the Mukhar formation were analyzed for Nd isotopes.The mafic rocks from the Ulgey bimodal suite have rather uniform radiogenic ε Nd(t) values ranging from +0.9 to +1.6, and the felsic samples have radiogenic ε Nd(t) values of +1.3-2.1.The basaltic samples from the Mukhar formation have significantly higher radiogenic ε Nd(t) values of +6.3 to +6.7.

Significance of the Results
The rhyolites collected from the Ulgey bimodal suite in this study yielded a zircon age of 415-410 Ma, which we interpret as the crystallization age of the bimodal volcanic suite from the Early Devonian Tunget formation.The youngest detrital zircon ages we found in the Mongol Altai formation (ca. 503 and 478 Ma) mark a maximum depositional age which is consistent with its previous estimated Late Cambrian-Early Ordovician age.The youngest zircon ages (391 Ma) in the Mukhar Formation suggest an Early Devonian age rather than Silurian.The samples from the Sagsai Formation yielded significantly younger zircon ages (379-351 Ma), indicating the sedimentation lasted at least until the Late Devonian-Early Carboniferous.The Precambrian detritus in the samples was potentially derived from the basement of the Mongolian continental blocks and their overlying Tonian continental arc magmatism (e.g., Badarch et al., 2002;Jiang et al., 2017).The Cambrian-Early Ordovician age populations match the ages of the Ikh-Mongol Arc System (570-460 Ma; Janoušek et al., 2018).We interpret the Early Devonian detrital zircon signature of the Mukhar and Sagsai formations to be derived from erosion of the bimodal volcanic suites.According to these new results, a revised stratigraphic column for the Ulgey region is shown in Figure S3 in Supporting Information S1.
In principle, crustal contamination could have affected the compositions of mantle-derived magmas.However, the lack of correlation of Nb/La and Th/ La, and of ε Nd(t) with SiO 2 rule out significant crustal contamination for the mafic rocks of the Ulgey bimodal suite (Figures S4a and S4b   mafic rocks can best be interpreted to be the result of varying degrees of partial melting of a depleted lithospheric mantle that was metasomatized by subduction-derived components. For the bimodal suite, two main models have been proposed for genesis of evolved felsic magma: (a) partial melting of crustal rocks (anatexis) or young underplated basalts (e.g., Frost et al., 2001;Mahoney et al., 2008); and (b) extensive fractional crystallization from common mantle-derived mafic magmas, with or without crust assimilation (e.g., Peccerillo et al., 2003).In the former model, the mafic and felsic rocks show distinctly different geochemical features and Sr-Nd isotopic ratios (e.g., McCurry & Rodgers, 2009).In the latter model, the mafic and felsic rocks would exhibit similar geochemical signatures and Sr-Nd isotopic compositions, with mafic rocks dominating volumetrically compared with felsic rocks.The rhyolite samples from the Ulgey bimodal suite are characterized by high silica and alkali contents, strong negative Eu anomalies, and high concentrations in Ga, Zr, Nb, Ce and Y, which are typical of geochemical features of A-type granites (Figure S6 in Supporting Information S1; e.g.Whalen et al., 1987), indicating they likely formed from partial melting of an anhydrous source (Collins et al., 2021).The absence of intermediate compositions and the larger volumes of the felsic rocks than the mafic rocks suggest that the felsic rocks were not likely formed by fractional crystallization from the coeval mafic magma.The felsic rocks have positive ε Nd(t) values (1.3-2.1), which are indistinguishable from the mafic rocks of the Ulgey bimodal suite, indicating that they were probably derived from partial melting of the underplated mafic rocks of the lower crust.
The lack of a correlation between Nb/La and Th/La, and ε Nd(t) with SiO 2 , and the low Th/Ce (0.05-0.06) and Th/ Ta (1.6-1.9)indicate negligible crustal contamination during the evolution of the basalts from the Mukhar formation (Figures S4a and S4b in Supporting Information S1).Their LREE enrichment and lack of Nb-Ta anomaly is similar to E-MORB, but they have higher REE contents than the typical E-MORB (Sun & McDonough, 1989).An E-MORB mantle source is further supported by all these basaltic samples falling in the E-MORB field on the Th/Yb versus Nb/Yb diagram (Figure 3g).The (La/Sm) N versus (Sm/Yb) N and Sm/Yb versus Sm diagrams imply that these E-MORB-like basalts formed by low degree partial melting (∼5%) of a mantle peridotite in the transitional spinel-garnet stability field (Figure S7 in Supporting Information S1).Thus, we interpret these E-MORB-like basalts with high positive ε Nd(t) to have formed from partial melting of a depleted mantle that was not metasomatized by subduction-related components (Figure 3g), which is distinct from the mantle source of the mafic rocks from the bimodal suite.

Tectonomagmatic Setting
Bimodal magmatic suites are characteristic extensional tectonic settings, including plume-related continental rifts, incipient back-arc basins, subduction zones and post-collisional extensional settings (e.g., Meade et al., 2014;Shinjo & Kato, 2000).The Ulgey bimodal suite formed nearby and at the same time as the Altay-Sayan Rift System (also termed the Altay-Sayan LIP) (ca.410-390 Ma; Figure 1), which is dominated by mafic volcanism and phonolites, trachytes, and commendites, as well as a bimodal volcanic suite with associated sediments (e.g., Izokh et al., 2011;Vorontsov et al., 2021).Coeval with this Altay-Sayan LIP/Rift system, an Early Devonian extensional regime associated with asthenospheric upwelling in the Chinese Altai region developed, accompanied by (a) newly formed extensional basins that contain bimodal volcanic suites (e.g., Chai et al., 2009), (b) high-temperature/low-pressure metamorphic terranes with extension-related sub-horizontal foliations (e.g., Jiang et al., 2022), (c) MORB-like mafic rocks and coeval S-type granites (e.g., Cai et al., 2010), (d) widespread deep crustal anataxis that produced migmatite-granite complex (Wang et al., 2021), (e) juvenile mantle source addition evidenced by the abrupt increase of zircon ε Hf(t) from various tectonic units (P.F. Li et al., 2019).There are three tectonic models proposed to explain the extensional environment indicated by all of these geologic features: ridge subduction (e.g., Cai et al., 2011), southward subduction retreat of the Paleo-Asian ocean (e.g., P. F. Li et al., 2019;Soejono et al., 2018), and the effects of a mantle plume (Ernst et al., 2020;Kravchinsky, 2012;Kuzmin et al., 2010;Vorontsov et al., 2021).The ridge subduction model requires some form of flat subduction that should have resulted in a compressional environment and tectonic erosion of the overriding plate (e.g., Antonijevic et al., 2015), which contradicts the widespread extensional features found in the Devonian rocks, and is inconsistent with the apparent absence of geochemically distinctive adakitic rocks (high MgO, Cr, Co and Ni contents) and N-MORB derived magmas (Wang et al., 2020).Slab rollback could result in back-arc extensions (e.g., Bercovici & Long, 2014), but is unable to explain the triple-junction configuration and within plate OIB-like basalts in the Altay-Sayan LIP/Rift System (Figure 3g; Vorontsov et al., 2021).Some extensional areas are remote (more than 1,000 km) from the subduction zone during Early Devonian (Figure 1).In addition, extension-related metamorphism and magmatism both occur in a broad region in a narrow time interval (420-380 Ma, peaking at ca. 400 Ma) and show no age migration trend (Cai et al., 2011;Chai et al., 2009;P. F. Li et al., 2019;Vorontsov et al., 2021), which is inconsistent with the slab rollback model.The Altay-Sayan LIP/Rift System encompasses a total area of 0.35 × 10 6 km 2 , and magmatism on different sites occurred nearly simultaneously (Ernst et al., 2020;Kuzmin et al., 2010).If our study area and Chinese Altay are included as part of this context, the lateral extent of the Early Devonian LIP would be larger than previously thought.The basaltic rocks in the Altay-Sayan LIP include both high-Ti and low-Ti varieties, similar to many LIPs such as for example, Siberian Traps and Karoo LIP of South Africa (Vorontsov et al., 2021).In addition, ca.407 Ma picrodolerites, considered to be important evidence for a mantle plume, are recognized in the center of a triple junction from the Altay-Sayan LIP/Rift System (Izokh et al., 2011;Kravchinsky, 2012).The mafic rocks with subduction features were likely derived from plume-induced melting of the lithospheric mantle that was previously metasomatized during the Early Paleozoic accretion/subduction event (Vorontsov et al., 2021).Taken together, the magmatism from the Altay-Sayan LIP/Rift was likely to have originated from the activity of mantle plumes (Kravchinsky, 2012; Kuzmin et al., 2010;Vorontsov et al., 2021).

Inception of the Wilson Cycle in the Accretionary Orogen
Mantle plumes are usually involved in the first stage of the Wilson cycle: breakup of continents and opening of ocean (e.g., Storey, 1995).In Northwest Mongolia, the Ulgey bimodal suite (410-415 Ma) likely documents initial continent rifting of the Early Paleozoic collage in the CAOB.As rifting continued, the basalts from the Mukhar formation (younger than 391 Ma) with E-MORB geochemical affinity likely result from partial melting of the upwelling asthenosphere influenced by the Early Devonian mantle plume.Thus, we suggest the basalts from the Mukhar Formation represent initial oceanic crust formation during early seafloor spreading, similar to the scenario of the young South China Sea where extensive E-MORB occurs along the seafloor (Larsen et al., 2018;Liao et al., 2022).In the Ereendavaa terrane along southern margin of the MOO, coeval bimodal volcanic rocks and alkaline riebeckite granites (418-409 Ma) document an Early Devonian extensional environment (Narantsetseg et al., 2019;Orolmaa et al., 2015).An extensional environment is also supported by the widespread occurrence of the Devonian diabase and gabbro-diabase sill swarms within the Early Devonian shallow marine molasse formations in this region (Narantsetseg et al., 2019), which is usually suggested to document continental lithospheric extension, continental rifting and breakup events (e.g., Bryan & Ernst, 2008).These records of extension are coeval with the Devonian Altay-Sayan LIP, suggesting the ascent of an Early Devonian mantle plume may have triggered the opening of the MOO.The age of the earliest rift-related sedimentation could provide constraints on the timing of continental breakup and the initiation of seafloor spreading.In the Ereendavaa terrane, the Neoproterozoic formations are unconformably overlain by Silurian clastic strata and Devonian volcanic and volcaniclastic rocks, and minor limestone (Badarch et al., 2002).Zircon U-Pb dating results indicate the Silurian-Devonian formation formed during latest Silurian-Early Devonian, probably related to the opening of the MOO (Miao et al., 2017).To the northeast, in the Jiamusi region of the Amuria block, the Middle Devonian Heitai Formation overlying the Precambrian basement consists of clastic rocks and carbonates, and is proposed to document the passive continental margin of the MOO at ca. 380 Ma (G.Y. Li et al., 2019).These records indicate that the MOO initially opened during Early Devonian and divided the Early Paleozoic collage of terranes previously assembled against the southeast margin of the Siberian Craton (Figure 4a).Paleomagnetic studies indicate that the Amuria blocks were located around Siberia during the Silurian, but differ by 30°in paleolatitude during the Devonian (Bretshtein & Klimova, 2007;Kravchinsky et al., 2002;Torsvik et al., 2012), indicating that the MOO between these terranes progressively widened by that time.Thus, we propose a new tectono-magmatic model in which the rising Devonian hot plume impinged upon the lithosphere of northern Early Paleozoic collage and further weakened and thinned the lithosphere to ultimately trigger the opening of the MOO.In addition, the MOO initiated between the microcontinents that accreted to Siberia Craton (Figure 1), likely because the microcontinental blocks with cratonic lithosphere represent rigid blocks within accretionary orogens (Zhou et al., 2018).The intervening weak orogenic lithosphere between the microcontinents guides the continent breakup and consequent ocean birth with the assistance of plume-induced lithospheric weakening.

Conclusions
The 415-410 Ma bimodal volcanic suite and associated volcanic-sedimentary rocks in northwest Mongolia comprise part of the Altay-Sayan LIP/Rift System, and represent a widespread Early Devonian extensional event Geophysical Research Letters 10.1029/2024GL109028 within the northern Early Paleozoic collage of the CAOB.This Devonian extension regime is attributed to a mantle plume, which is thought to have impacted and weakened the lithosphere of northern Early Paleozoic collage ultimately leading to the opening of the MOO.Our model of MOO opening implies that the continent breakup in accretionary orogens tends to take place along intervening weak orogenic lithosphere between the rigid microcontinents.

Figure 1 .
Figure 1.Tectonic map of Central Asia showing the positions of Altai-Sayan LIP/Rift System and Mongol-Okhotsk orogenic belt within the Central Asian Orogenic Belt (Modified fromZhou et al., 2018;Vorontsov et al., 2021).

Figure 2 .
Figure 2. Field occurrences and zircon U-Pb results for the Ulgey bimodal volcanic suite and associated formations.(a) The Ulgey bimodal volcanic suite; (b) basalts from the Silurian Mukhar formation; (c) zircon U-Pb concordia plots of the two rhyolites from the Ulgey bimodal suite; (d) detrital zircon U-Pb ages for the Cambrian-Devonian sedimentary rocks.
in Supporting Information S1).The mafic rocks have higher SiO 2 contents, but lower Mg # , Cr, and Ni contents than those of the primitive mantle-derived magma, suggesting variable amounts of fractional crystallization.The positive correlation of Cr and Ni contents against Mg # , and Ni versus Cr and V versus Cr diagrams indicate the likelihood of the fractional crystallization of olivine and clinopyroxene (Figures S5a-S5d in Supporting Information S1).The lack of correlation between the Dy/Yb ratios and SiO 2 contents, and between TiO 2 and MgO contents imply that amphibole and Fe-Ti oxide fractionation did not play a major role during the magmatic evolution (Figures S5e and S5f in Supporting Information S1).The mafic rocks from the Ulgey bimodal suite have low (La/Yb) N (2.1-5.6) and (Tb/Yb) N (1.04-1.35)ratios, and high HREE contents, indicating they were derived by partial melting of shallow spinel-bearing peridotites (Rooney, 2010).They are characterized by negative Nb, Ta, and Ti anomalies, are enriched in LILE, and plot above the MORB-OIB array (Figure3g), suggesting their mantle source was modified by subduction-driven metasomatism (e.g.,Clift et al., 2009;Gill, 1981;Pearce et al., 2021).In summary, the arc signatures and the positive ε Nd(t) for

Figure 3 .
Figure 3. Geochemical plots of the Ulgey bimodal volcanic suite and the basalts from the Silurian Mukhar formation.(a, b) Primitive-mantle normalized diagrams and chondrite-normalized REE patterns for the mafic rocks from the Ulgey bimodal volcanic suite; (c, d) Primitive-mantle normalized diagrams and chondrite-normalized REE patterns for the felsic rocks from the Ulgey bimodal volcanic suite; (e, f) Primitive-mantle normalized diagrams and chondrite-normalized REE patterns for the basalts from the Silurian Mukhar formation; (g) Th/Yb-Nb/Yb diagram (J. A. Pearce, 2008) for the mafic rocks from the Ulgey bimodal suite, the Silurian Mukhar formation and the Altay-Sayan LIP/Rift System.Normalizing values are from Sun & McDonough (1989) for both chondrite and primitive mantle.The data of the Altay-Sayan LIP/Rift System are from Vorontsov et al. (2021) for comparison.