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Two dolerite dyke swarms are recognized along and paralleling the Ural Mountains, Russia. The Uralian swarm is 1400-km long (2300-km long if traced from its inferred plume centre). Further north, the Pay-Khoy swarm can be traced through the Pay-Khoy–Novaya Zemlya fold belt for a distance of c. 250 km (800-km long if traced from its inferred plume c...
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... at the University of Toronto, where selected grains were then analysed using stand- ard isotope dilution thermal ionization techniques (e.g. Hamilton & Buchan 2010). Three fractions of baddeleyite were analysed, each comprising between four and eight grains; U-Pb isotopic results are presented in Table 1. Data are presented in graphical form in Fig. 4. The results for all three fractions are entirely over- lapping, and straddle Concordia. Calculated Th/U ratios' range is from 0.08 to 0.19; the slightly elevated values suggest possi- ble minor overgrowth by either late magmatic or metamorphic zircon, though this is not obvious via optical microscopy and hardly influences the results. ...
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... Paleozoic magmatism in the East European (Baltica) Craton (including in the Timanides, Fig. 1) is usually assigned to the Middle-Upper Devonian, with a predominance of activity in the Upper Devonian. This extensive Devonian magmatic activity was widespread across the East European Craton (e.g. Nikish- in et al. 1996; Fig. 54 in Puchkov 2010; Fig. 11 Upper Devonian and therefore potentially part of the same LIP. The structural setting of the Kola Alkaline Province was recently reinvestigated by Terekhov et al. (2012), who demonstrated de facto (their Fig. 8) that the magmatism extended even farther north, into the East Barents Sea basin. Like the Pricaspian ...
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... but voluminous pulse of volcanism is accompanied in the Novaya Zemlya region by a sudden change from shelf to deep water sedimentation. This sea-level change was possibly connected with rift processes in the adjacent East Barents basin ( Fig. 1), likely resulting in intense destruction (rifting and thinning) of its crystalline crust (Terekhov et al. 2012; Puchk- ov 2013b). The NW-trending dyke swarm on the Vaigach island and the Pay-Khoy Range − where Devonian deposits are partly eroded − is mainly hosted by Ordovician sediments. The dolerite dykes and large folded sills in the central part of the Pay-Khoy anticlinorium are aligned en echelon and almost parallel to the axis of the anticlinorium. This alignment may, however, have been enhanced during subsequent Late Paleozoic folding. How- ever, the current trend of the swarm is considered nearly primary (see paleomagnetic discussion below). Associated sills are differ- entiated and deformed into large mapable folds. The number of dykes and sills decrease markedly up-section, to the flanks of the anticlinorium. Numerous K–Ar dates scatter from Ordovician to Triassic (455 ± 5 to 249 ± 11 Ma), partly due to syn-orogenic heating and deformation, making the true age of the dykes and sills ambiguous (Shaibekov 2012, and references therein). The most reliable U–Pb (SHRIMP) age is determined on zircon from a layered gabbro–dolerite sill at Mount Sopcha-Myl’k, inside the axial zone of the Pay-Khoy anticlinorium: 369.8 ± 2.3 Ma and 370.3 ± 2.3 (Lower Famennian) (Shaibekov 2012). This age is supported by Shishkin et al. (2009), who provide addition- al U–Pb SHRIMP zircon age determinations (374.6 ± 2.0 and 381.4 ± 2.0 Ma, i.e. Frasnian) of dolerites in the “First Uchastok” area, located ~15 km to the SE from Sopcha-Mylk. Sample KV2 was collected at 58°21 25.7 N & 57°52 17.5 E (area #7 in Fig. 2) from a railway cut, west of Skalny railway station, within the Kvarkush anticlinorium of the Middle Urals. This outcrop exposes a dark grey to black, NNW-striking, medi- um-grained gabbro–dolerite dyke that is at least 50–60-m thick (its eastern contact is truncated by faulting). The dyke is mod- erately affected by low-grade alteration. The western contact is undeformed and has a chilled margin that dips 65–70°E. A sample collected for geochronology was taken from the approx- imate dyke centre, roughly 30 m from the chilled margin on the western side. The dyke cuts polymictic siltstones and sandstones of the Chernokamensk Formation, which is interpreted to be Upper Vendian in age. The Formation contains Ediacaran-type fauna Arumberia banksi and Pteridinium simplex, collected by Puchkov (2012b) and identified by V. Grazhdankin. The geolog- ical field relationships therefore constrain the dyke to be young- er than Upper Vendian in age. This geological context was the reason behind the sample being collected for U–Pb dating, to provide a precise age on the Uralian swarm. Sample crushing and mineral separation were carried out at Lund University according to the procedures outlined in Söderlund and Johansson (2002). Approximately, 60 pale to medium-brown blades and blade fragments of baddeleyite were recovered; the vast majority of the crystals had a maximum dimension of about 35 μ. Best-quality baddeleyite crystals were hand-picked under ethanol with a binocular microscope at the Jack Satterly Geochronology Laboratory at the University of Toronto, where selected grains were then analysed using stand- ard isotope dilution thermal ionization techniques (e.g. Hamilton & Buchan 2010). Three fractions of baddeleyite were analysed, each comprising between four and eight grains; U–Pb isotopic results are presented in Table 1. Data are presented in graphical form in Fig. 4. The results for all three fractions are entirely over- lapping, and straddle Concordia. Calculated Th/U ratios’ range is from 0.08 to 0.19; the slightly elevated values suggest possi- ble minor overgrowth by either late magmatic or metamorphic zircon, though this is not obvious via optical microscopy and hardly influences the results. Pb loss is not apparent, as 206 Pb/ 238 ...
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Karavannoe is a pallasite found in Russia in 2010. The mineralogy, chemistry, and oxygen isotopic composition indicate that Karavannoe is a member of the Eagle Station Pallasite (ESP) group. Karavannoe contains mostly olivine and subdued interstitial Fe,Ni‐metal. Zoned distribution of FeO in small, rounded grains of olivine and FeO and Al2O3 in chr...
Citations
... Devonian magmatism within the East European craton, including the Azov and Archangelsk regions, can be grouped as the Kola-Dnieper Large Igneous Province (LIP) (Ernst, 2014) with two proposed mantle plume centres (Puchkov et al., 2016), (1) a southern centre at the intersection of the Prypyat-Dnieper-Donets paleorift and the Uralian dyke swarm and, (2) a northern centre in the Barents Sea near Novaya Zemlya, at the convergence between the Pay-Khoy dyke swarm and a swarm extending from the northern coast of the Kola Peninsula, as well as at the convergence of rift/graben zones. Furthermore, this Kola-Dnieper LIP with its two plume centres is approximately coeval with the Yakutsk-Vilyui LIP and its plume centre on the eastern side of the Siberian Craton. ...
... Furthermore, this Kola-Dnieper LIP with its two plume centres is approximately coeval with the Yakutsk-Vilyui LIP and its plume centre on the eastern side of the Siberian Craton. These two LIPs were in close proximity at that time and their three plumes (two below the Eastern European craton and one below Siberia) may represent branches of a superplume derived from an active part of a single deep mantle LLSVP (Large Low Shear-Wave Velocity Province), the so-called Tuzo superswell (Puchkov et al., 2016). The presence of coeval kimberlite magmatism provides additional support for a plume origin for the Kola-Dnieper LIP. ...
Zircon megacrysts are commonly found in kimberlites and, together with olivine, low-Cr garnet, pyroxene, phlogopite, and ilmenite megacrysts, they constitute a mineral assemblage known as the “low-Cr suite”. The generally close similarity of ages and similar isotope geochemical characteristics of megacrysts and matrix minerals in the host kimberlites support a cognate origin. However, alteration rims commonly develop on zircon and ilmenite megacrysts, providing evidence for a lack of chemical equilibrium between the megacrysts and kimberlitic melts. Here, we report results of a detailed geochronological and geochemical study of zircon megacrysts found in the Middle Devonian Novolaspa kimberlite pipe and dyke located in the Azov Domain of the Ukrainian Shield. The concordia age of zircons is 397.0 ± 2.0 Ma, and it is 14 m.y. older than the age of kimberlite emplacement as defined by a Rb-Sr isochron on phlogopite. The average εHf(397) value for unaltered zircon megacrysts is 6.8 ± 0.14, with the alteration rims having similar Hf isotope systematics. These hafnium isotope data indicate a moderately depleted mantle source for zircon. Unaltered megacrystic zircons have low abundances of trace elements and fractionated REE, with pronounced positive Ce/Ce* anomalies and almost no Eu/Eu* anomalies. In contrast, alteration rims have very high and variable concentrations of trace elements, indicating a reaction between zircon and kimberlite melt. The melt or fluid responsible for zircon and ilmenite megacryst formation, in contrast to kimberlitic melt, was poor in incompatible trace elements, except for the HFSE (Zr, Hf, Nb, Ta, and Ti). The oxygen fugacity during crystallization of the megacryst suite was close to the FMQ buffer.
Azov zircon megacrysts do not demonstrate close geochronological and isotope-geochemical similarities with their host kimberlites. They are cognate in the broad sense of being related to the same plume event, but their direct affinity is not clearly defined. The megacryst suite may have crystallized from the earliest melts/fluids that separated from the ascending mantle plume, whereas kimberlite magmas were emplaced 14 m.y. after this event.
... Stephenson et al., 2006). In this regard, Puchkov et al. (2016) suggested the DDB could be linked to a mantle plume centred further to the southeast of its termination than envisaged by Zonenshain et al (1990) and manifest as part of an EEC-wide "Kola-Dnieper" Large Igneous Province (Ernst, 2014). ...
This paper analyses the role of pre-existing Precambrian structures for the localisation of the intracratonic rifts from a case study of the Dniepr-Donets Basin (DDB) in Ukraine. The DDB was formed as a result of Late Palaeozoic rifting in the Archaean-Paleoproterozoic Sarmatian segment of the East European craton (EEC). It separates the Ukrainian Shield (UkS) to its southwest from the Voronezh Massif (VM) to its northeast. The Donbas Foldbelt (DF) constitutes the tectonically inverted part of the DDB in its southeastern extent and has been imaged by coincident wide-angle reflection and refraction seismic as well as deep near-vertical reflection seismic profiles (project “DOBRE”). It is almost completely filled with a highly indurated succession of upper Palaeozoic sediments and metasediments, up to some 20 km in thickness, now exposed at the surface. Here, a crustal and upper mantle structural-compositional model that is tightly constrained by the seismic data and gravity anomalies along the profile is used to search for Precambrian pre-rift crustal features that could have played a role in localising Late Palaeozoic rifting. The results suggest that there may be a different tectonic history for Sarmatian crystalline crust on either side of the DF. Density isolines in the AM crust are shallower than corresponding ones of equal value in the VM crust and, accordingly, the mean density of the crust of the AM is higher. This effect, calibrated on the DOBRE profile, is expressed along the margins of the entire DDB with a higher background level of the gravity field seen generally for the UkS than for the VM. The associated gravity gradient coinciding with the location of Palaeozoic rifting means that there is a perturbation to the horizontal deviatoric stress in this position that likely predates rifting. Further, a well-constrained upper crustal low-density granitic body beneath the northeastern flank of the DF produces a significant negative gravity anomaly superimposed upon the background gravity gradient. This adds a significant additional extensional component to the ambient deviatoric stress field. It cannot be concluded with certainty that either of these crustal features was necessary or sufficient for “seeding” Late Palaeozoic rifting but modern passive seismology surveys across the DDB as well as new bedrock geological studies would help test such a hypothesis.
... Significant REE-U-Th-Ta-Zr-Nb mineralisation (~ 80 Mt at 0.6-1.1% TREO) is documented at the margins and roof of the Motzfeldt intrusion (Tukiainen, 2014). Other notable alkaline intrusions include the Khibina, Lovozero, Kurga, and Niva syenitic plutons of the Kola Alkaline Carbonatite Province, which in turn is part of the Kola-Dnieper LIP (Puchkov et al., 2016), of Russia and eastern Finland (see Downes et al., 2005 and references therein). The Khibina massif comprises one of the world's largest apatite deposits, which also comprises considerable amounts of SrO (~ 4.5 wt%) and REE 2 O 3 (< 8.891 ppm; Arzamastsev et al., 1987;Kogarko, 2018). ...
In the present paper, we have compiled data on 565 layered and differentiated igneous intrusions globally, documenting their (i) location, (ii) age, (iii) size, (iv) geotectonic setting, (v) putative parent magma(s), (vi) crystallisation sequence, and (vii) mineral deposits. Most studied intrusions occur in Russia (98), Australia (72), Canada (52), Finland (37), South Africa (38), China (33), and Brazil (31). Notable clusters of: (i) Archaean intrusions (~ 15%) include those of the McFaulds Lake Area (commonly known as the Ring of Fire, Canada), Pilbara and Yilgarn cratons (Australia), and Barberton (South Africa); (ii) Proterozoic intrusions (~ 56%) include those of the Giles Event and Halls Creek Orogen (Australia), Kaapvaal craton and its margin (South Africa and Botswana), Kola and Karelia cratons (Finland and Russia), and Midcontinent Rift (Canada and USA); and (iii) Phanerozoic intrusions (~ 29%) include those of eastern Greenland, the Central Asian Orogenic Belt (China and Mongolia) and Emeishan large igneous province (China). Throughout geological time, the occurrence of many layered intrusions correlate broadly with the amalgamation and break-up of supercontinents, yet the size and mineral inventory of intrusions shows no obvious secular changes.
In our compilation, 337 intrusions possess one or more types of mineral occurrences, including: (i) 107 with stratiform PGE reef-style mineralisation, (ii) 138 with Ni-Cu-(PGE) contact-style mineralisation, (iii) 74 with stratiform Fe-Ti-V-(P) horizons, and (iv) ≥ 35 with chromitite seams. Sill-like or chonolithic differentiated intrusions present in extensional tectonic settings and spanning geological time are most prospective for Ni-Cu-(PGE) mineralisation. In contrast, PGE reef-style deposits are most prevalent in larger, commonly lopolithic intrusions that are generally >1 Ga in age (~ 75%). Stratiform Fe-Ti-V-(P) horizons are most common in the central and upper portions of larger layered intrusions, occurring in the Archaean and Phanerozoic. Approximately 80% of intrusions with chromitite seams are older than 1 Ga and > 50% of them also contain PGE reefs.
Based on the distribution of layered intrusions in relatively well explored terranes (e.g., Finland, South Africa, Western Australia), we propose that many layered intrusions remain to be discovered on Earth, particularly in poorly explored and relatively inaccessible regions of Africa, Australia, Russia, Greenland, Antarctica, South America, and northern Canada.
... Another possible cause for the Devonian rifting and magmatism that occurred across the East European Craton is rise of a mantle plume (Nikishin et al. 1996;Puchkov et al. 2016). ...
Timan-Pechora Composite Tectono-Sedimentary Element represents a significant part of the Timan-Pechora petroleum province, which is the second largest in the Circum-Arctic. It contains as much as up to 10 km of Paleozoic and Mesozoic strata hosting world-class hydrocarbon source rock, the Domanik Formation, and a variety of hydrocarbon plays prolific for both, oil and natural gas. Complex tectonic structure of the composite tectono-sedimentary element formed as result of several tectonic phases: two extensional events, post-rift thermal sag in a passive margin setting, and a series of late Paleozoic and early Mesozoic compressional events. The latter modified the extensional fabric and led to the formation of a number of inverted swells and smaller anticlinal structures providing the major trapping capacities. The deposition of source and reservoir facies occurred during the extensional tectonic phases, while the main reservoir-prone sedimentary units were deposited during late Paleozoic and early Mesozoic orogenic phases.
... The ca. 370 Ma Kola-Dnieper LIP of Baltica (also known as the East European craton) includes coeval mafic magma tism of the Dnieper-Donets rift, a dyke swarm extending for 2,000 km along the Urals, and magmatism in the Kola pen insula and elsewhere in the Baltic craton (Nikishin et al., 1996;Kravchinsky, 2012;Puchkov et al., 2016). Two plume centers are recognized (Puckhov et al., 2016). ...
Earth has gone through periods of cooling including global, near global, or regional glaciations, which are observed in the Archean, Paleoproterozoic, Neoproterozoic, Ordovician, Permo‐Carboniferous, and Cenozoic times. We review the mechanisms by which large igneous provinces (LIPs) and silicic LIPs (SLIPs) can cause global cooling. Then we investigate the correlation of LIPs with important glaciation events, focusing on those of Neoproterozoic and Phanerozoic age. The 720 Ma Franklin‐Irkutsk LIP, a large part of which was emplaced into an evaporite basin and all of which was emplaced in the tropics, is linked with the start of the Sturtian glaciation, one of the longest and most severe glaciations in Earth history. The ca. 579 Ma pulse of the Central Iapetus Magmatic Province (CIMP) is associated with the start and end of the Gaskiers glaciation. The Hirnantian glaciation (ca. 440 Ma) may be associated with poorly dated ca. 450 Ma intraplate magmatism in several regions, including eastern Siberia, South Korea, Argentina, Iran, and elsewhere. It is also coincident with a huge volume of silicic volcanic provinces generated by supereruptions. Permo‐Carboniferous glaciations (P1–P4, 300–260 Ma) can be correlated with widespread intraplate magmatism of the European northwest African magmatic province (and its initiation as the 300 Ma Skagerrak LIP), and also the 259 Ma Emeishan LIP of China. A recently recognized ca. 34 Ma initial pulse of the Afro‐Arabian LIP matches the Eocene‐Oligocene cooling (Oi‐1 glaciation). More precise dating of both the LIPs and cooling events is required to confirm the correlations and to assess the role of LIPs relative to other causes proposed for global and regional glaciations.
... Некоторое обогащение этих комплексов крупноионными и литофильными элементами (Ba, Sr, Pb, Th и др.) и деплетированность Nb и Та можно объяснить выплавлением магм в пределах верхней мантии, прошедшей длительную эволюцию в надсубдукционной обстановке, как это делается, например, в работе [3], при характеристике изменений состава магматических пород при переходе от субдукционных обстановок к внутриплитным. Нельзя также исключить вероятность теплового воздействия девонского Кольско-Днепровского мантийного суперплюма, магматические проявления которого известны на западном склоне Урала [18], как одной из причин формирования постаккреционных магматических комплексов на востоке Урала. ...
The study of the geochemical features and isotopic (Sm-Nd and U-Pb) age of the Ivdel dolerite complex distributed on the eastern slope of the Northern Urals within the Tagil island-arc megazone was performed. It was found that the magmatic rocks composing it are of Famenian age and, consequently, were formed after the closure of the subduction zone. The rocks of the Ivdel complex show similarities to volcanites of both convergent and divergent environments, and probably formed from the products of partial melting of the depleted suprasubduction upper mantle. Famennian hypabyssal-subvolcanic and volcanogenic complexes, similar to the Ivdel complex, are also known in island-arc blocks in the Circumpolar and Southern Urals.
... The Devonian stage in the central and southern parts of the EEP was responsible for the rejuvenation of numerous deep-seated faults and regeneration of aulacogens (Dnieper-Donets, Kirovsk, Don-Medveditsa), with their repeated downwarping (Grushevoi et al., 1996;Ivanova and Grushevoi, 2009). Devonian activation is peculiar in the manifestation of alkali basalts, trachybasalts, and alkali-ultrabasic intrusions in the marginal parts of the mentioned aulacogens (e.g., Petrov, 1969;Puchkov et al., 2016), including the southern (Dnieper-Donets area) and eastern (Don-Medveditsa area) flanks of the ore field. Basaltic rift volcanism spanned a spacious area in the central and eastern parts of the Russian Plate and formed the Devonian East European Large Igneous Province (LIP) (Milanovsky, 1996;Nikishin et al., 2002;Puchkov, 2002;Ernst and Bell, 2010). ...
... Basaltic rift volcanism spanned a spacious area in the central and eastern parts of the Russian Plate and formed the Devonian East European Large Igneous Province (LIP) (Milanovsky, 1996;Nikishin et al., 2002;Puchkov, 2002;Ernst and Bell, 2010). Intense basaltic volcanism was noted in the Middle-Late Devonian in the Donets Basin (Puchkov, 2010). This superplume activity "rejuvenated" the structures of the East European LIP, in particular, the Pachelma aulacogen and its framing, and renovated basement faults, thus providing the drainage of the deeper crustal interior. ...
... Activation of basement faults and deformation of sedimentary cover during the Phanerozoic likely reflected both deep-seated geodynamic processes in the lower crust of the EEP and tectonic evolution in the adjacent fold areas: multiple collisional events in the Urals in the second part of the Paleozoic, as wells as in the Jurassic (Puchkov, 2010) and in the Alpine-Himalayan system in the Meso-Cenozoic. As suggested by (Grushevoi et al., 1996), aulacogens and updip traced bordering faults at the plate stage were tectonically weakened zones, which could serve as pathways for the ascending thermal waters (ore-bearing solutions). ...
Briketno–Zheltukhinskoe U–Mo–Re deposit in southern sector of the Moscow Lignite Basin (central part of the East European platform) localized in paleo-channel and deltaic coal-bearing sandy sediments of the Bobrikovsky horizon of Visean age, lying on the Famennian limestone, and covered by younger Neogene–Quaternary sand and clay. In tectonic terms, the position of the deposit corresponds to the South shoulder of the Pachelma Aulacogen, cross-sected by SN-trending fault zone. The presence of a thick gray-colored unit of mixed-grained moderately and poorly sorted sands containing carbonaceous plant detritus is among the lithologic-facies factors of localization of U-Mo-Re mineralization. Sand-dominated Bobrikovsky series has accumulated in fluvial, swamps inland, onshore delta-plain and shallow-sea lagoonal environments on the background of a warm humid climate. A combined syn-epigenetic formation model of the U–Mo–Re paleovalley type deposit is proposed. Subeconomic stratabound U (±Mo, Re) mineralization associated with carbonaceous and clayey horizons was accumulated during sedimentation and at the stage of diagenesis. During epigenesis, U–Mo–Re ores were deposited by oxidized groundwater as a result of their lateral filtration through highly permeable sand horizons and metal concentrations at the reduction and sorption barriers. The general subhorizontal stratiform structure of the ore deposit is complicated by the presence of sub-vertical morphological (swell of sand horizon plus strong pyritization) and concentration (Re+Mo column-like maximums) ore shoots. They occur in domed structures that disturb the horizontal structure of the host sedimentary unit. It is possible that these domes and ore shoots are the result of hydrothermal-hydraulic processes caused by the activity of deep crustal (and taking into account the renium-abundance and mantle?) fluids.
... Composite timing of the Late Devonian volcanism, presented separately for large igneous provinces (LIPs; light red; overall temporal range after Ernst et al., 2020) and arc magmatism (dark red), with emphasis on eruptive pulses of flood basalts (yellow circular-elliptical varieties) and explosive outbursts (stars); compiled from Ivanov (2015) and Tomshin et al. (2018) [Viluy; see Fig. 12B], Wilson and Lyashkevich (1996), fig. 2), Aizberg et al. (2001), fig. 1) [Pripyat-Dnieper-Donets; PDD, see Fig. 13], Larionova et al. (2016), Arzamastsev et al. (2017) and Arzamastsev (2018) [Kola], Puchkov et al. (2016) [Ural -Pay Khoy], Ernst (2014) and Ernst et al. (2020) [Maritimes SLIP?], and Winter (2015), fig. 2) [amplified arc volcanism]. ...
... Thus, the basalt effusions either signaled or coincided with the onset of the alkaline melting in the magmatic-rift system, in contrast to other LIPs (Arzamastsev et al., 2017). The Late Devonian effusive rocks were likely much less voluminous than other Late Devonian traps (Kravchinsky, 2012;Bond and Wignall, 2014), although they were also widely distributed as submarine volcanism in the basement of the Barents Sea (Nikishin et al., 1996;Puchkov et al., 2016). ...
... The PDD rift-volcanic system is usually linked with a mantle plume with its center located at the intersection of the Dnieper-Donets rift and the Uralian swarms (Puchkov et al., 2016). The last structure of the 370-377 Ma age is possibly even~2300 km long because it can be traced along the Ural Mountains to the Pay-Khoy-Novaya Zemlya fold belt. ...
Although the prime causation of the Late Devonian Frasnian–Famennian (F–F) mass extinction remains conjectural, such destructive factors as the spread of anoxia and rapid upheavals in the runaway greenhouse climate are generally accepted in the Earth-bound multicausal scenario. In terms of prime triggers of these global changes, volcanism paroxysm coupled with the Eovariscan tectonism has been suspected for many years. However, the recent discovery of multiple anomalous mercury enrichments at the worldwide scale provides a reliable factual basis for proposing a volcanic–tectonic scenario for the stepwise F–F ecological catastrophe, specifically the Kellwasser (KW) Crisis. A focus is usually on the cataclysmic emplacement of the Viluy large igneous province (LIP) in eastern Siberia. However, the long-lasted effusive outpouring was likely episodically paired with amplified arc magmatism and hydrothermal activity, and the rapid climate oscillations and glacioustatic responses could in fact have been promoted by diverse feedbacks driven by volcanism and tectonics. The anti-greenhouse effect of expanding intertidal–estuarine and riparian woodlands during transient CO2-greenhouse spikes was another key feedback on Late Devonian land. An updated volcanic press-pulse model is proposed with reference to the recent timing of LIPs and arc magmatism and the revised date of 371.9 Ma for the F–F boundary. The global changes were initiated by the pre-KW effusive activity of LIPs, which caused extreme stress in the global ecosystem. Nevertheless, at least two decisive pulses of sill-type intrusions and/or kimberlite/carbonatite eruptions, in addition to flood basalt extrusions on the East European Platform, are thought to have eventually led to the end-Frasnian ecological catastrophe. These stimuli have been enhanced by effective orbital modulation. An attractive option is to apply the scenario to other Late Devonian global events, as evidences in particular by the Hg spikes that coincide with the end-Famennian Hangenberg Crisis.
... This rifting was caused by subduction along the Laurussia border (Golonka and Gawęda, 2012), as well as Cameroon and Jebel Mara plums' activity (Fig. 2). Volcanics are abundant in the Dnepr-Donetsk-Pripyat rift Lyashkevich, 1996, Bush andKalmykow, 2005), Voronezh uplift (Yutkina et al., 2017) and Urals (Puchkov et al., 2016). ...
This paper presents Late Devonian (Frasnian–Famennian) global and regional paleogeographic maps displaying present day coastlines, tectonic elements’ boundaries, subductions, rifts, spreading centers, transform faults, paleogeographic configuration and volcanism 370 million years ago. The regional maps illustrate the paleoenvironment and paleolithofacies distribution.
The Late Devonian was a time of the onset and development of a major collisional event, the Variscan orogeny. The trench-pulling (or slab-pull) effect of the north dipping subduction, which developed along the Laurussia margin, caused the creation of the back-arc Rheno-Hercynian basin, as well as the transfer of tectonic elements. These tectonic elements included Saxothuringian, Southern Proto-Carpathian and Balkan terranes. The Antler and Ellesmerian orogenies constituted major collisional events in North America.
The spreading of the Paleotethys Ocean constituted the main extensional event. This spreading is associated with the movement of tectonic elements towards Laurussia, Siberia and Northern Kazakhstan. In addition, a branch of the Paleotethys Ocean was opened between South China and Gondwana, during the Late Devonian times. The spreading was displayed along the proto-Andean margin of western Gondwana and is thought to have opened the newly proposed Chilean Ocean. The development of major rift systems took place throughout Laurussia and Siberia. Late Devonian rifting was associated with volcanic activity, especially prominent in the Viluy rift in Siberia. The deposition, during the Late Devonian time, is characterized by the existence of large carbonate platforms with reefs on large continents and synorogenic flysch in collisional areas. The sea-level dropped towards the Devonian- Carboniferous boundary. The climate was undergoing change from greenhouse to icehouse.
The following plate tectonic events could have influenced the extinction of biotas at the Frasnian-Famennian boundary:
1) The very extensive basaltic volcanism in Laurussia and Siberian and along the arcs.
2) The closure of the Rheic Ocean and the development of the Variscan orogeny.
3) Intensive spreading in the Paleotethys and the development of numerous subductions and volcanic arcs.
These events resembled a transition from a rift to a drift phase, during the Permian–Mesozoic break-up of Pangaea. This break-up was associated with other biota extinctions.
... Рис. 4. Стратиграфическая колонка сылвицкой серии Кваркушско-Каменногорского поднятия; мощности показаны вне масштаба (по Аблизин и др., 1982; Гражданкин и др., 2010). Yesipov, Mladshikh, 1966;Roslyakova, Yesipov, 1966;Ablizin et al., 1982;Karta.., 1983;Becker, 1977, Grazhdankin et al., 2010Kolesnikov et al., 2012;Puchkov et al., 2016); B -scheme of the geological structure of the lower reaches of the basin Koiva River (according to Becker, 1980;Puchkov et al., 2016); C -scheme of geological structure of the lower reaches of the Sylvitsa River basin (according to Roslyakova et al., 1967;Grazhdankin et al., 2005Grazhdankin et al., , 2010Puchkov et al., 2016); legend: 1 -Lower Permian terrigenous-carbonate deposits; 2 -Carboniferous carbonate and terrigenous-carbonate deposits; 3 -Devonian terrigenous-carbonate deposits; 4 -Upper Ordovician -Lower Silurian terrigenous-carbonate deposits, more rarely -basic effusive ones; 5-9 -deposits of the Sylvitsa group: 5 -Ust-Sylvitsa formation, 6 -Chernyi Kamen formation, 7-9 -Staropechny and Perevalok formations: 7 -non dissected ones, 8 -Perevalok formation, 9 -Staropechny formation; 10 -Serebryanaya group deposits with the intersecting bodies of the Pre-Paleozoic intrusions, non dissected ones; 11 -deposits of the Basega group of the Upper Riphean; 12 -Post Early Carboniferous dikes of alkaline picrites; 13 -Late Devonian dikes of gabbro-dolerites; 14 -boundaries: a -tectonic, b -geological; 15: a -strike and dip of strata, b -position and numbers of localities of macrofossils. Localities of macrofossils: 1 -Shirokovskoe-1, 2 -Shirokovskoe-2, 3 -Usva-Vilukha, 4 -Usva-Krutikha, 6 -Koiva, 7 -Sylvitsa-1, 8 -Sylvitsa-2, 9 -Sylvitsa-3, 10 -Sylvitsa-4, 11 -Sylvitsa-5. ...
... Рис. 4. Стратиграфическая колонка сылвицкой серии Кваркушско-Каменногорского поднятия; мощности показаны вне масштаба (по Аблизин и др., 1982; Гражданкин и др., 2010). Yesipov, Mladshikh, 1966;Roslyakova, Yesipov, 1966;Ablizin et al., 1982;Karta.., 1983;Becker, 1977, Grazhdankin et al., 2010Kolesnikov et al., 2012;Puchkov et al., 2016); B -scheme of the geological structure of the lower reaches of the basin Koiva River (according to Becker, 1980;Puchkov et al., 2016); C -scheme of geological structure of the lower reaches of the Sylvitsa River basin (according to Roslyakova et al., 1967;Grazhdankin et al., 2005Grazhdankin et al., , 2010Puchkov et al., 2016); legend: 1 -Lower Permian terrigenous-carbonate deposits; 2 -Carboniferous carbonate and terrigenous-carbonate deposits; 3 -Devonian terrigenous-carbonate deposits; 4 -Upper Ordovician -Lower Silurian terrigenous-carbonate deposits, more rarely -basic effusive ones; 5-9 -deposits of the Sylvitsa group: 5 -Ust-Sylvitsa formation, 6 -Chernyi Kamen formation, 7-9 -Staropechny and Perevalok formations: 7 -non dissected ones, 8 -Perevalok formation, 9 -Staropechny formation; 10 -Serebryanaya group deposits with the intersecting bodies of the Pre-Paleozoic intrusions, non dissected ones; 11 -deposits of the Basega group of the Upper Riphean; 12 -Post Early Carboniferous dikes of alkaline picrites; 13 -Late Devonian dikes of gabbro-dolerites; 14 -boundaries: a -tectonic, b -geological; 15: a -strike and dip of strata, b -position and numbers of localities of macrofossils. Localities of macrofossils: 1 -Shirokovskoe-1, 2 -Shirokovskoe-2, 3 -Usva-Vilukha, 4 -Usva-Krutikha, 6 -Koiva, 7 -Sylvitsa-1, 8 -Sylvitsa-2, 9 -Sylvitsa-3, 10 -Sylvitsa-4, 11 -Sylvitsa-5. ...
... Рис. 4. Стратиграфическая колонка сылвицкой серии Кваркушско-Каменногорского поднятия; мощности показаны вне масштаба (по Аблизин и др., 1982; Гражданкин и др., 2010). Yesipov, Mladshikh, 1966;Roslyakova, Yesipov, 1966;Ablizin et al., 1982;Karta.., 1983;Becker, 1977, Grazhdankin et al., 2010Kolesnikov et al., 2012;Puchkov et al., 2016); B -scheme of the geological structure of the lower reaches of the basin Koiva River (according to Becker, 1980;Puchkov et al., 2016); C -scheme of geological structure of the lower reaches of the Sylvitsa River basin (according to Roslyakova et al., 1967;Grazhdankin et al., 2005Grazhdankin et al., , 2010Puchkov et al., 2016); legend: 1 -Lower Permian terrigenous-carbonate deposits; 2 -Carboniferous carbonate and terrigenous-carbonate deposits; 3 -Devonian terrigenous-carbonate deposits; 4 -Upper Ordovician -Lower Silurian terrigenous-carbonate deposits, more rarely -basic effusive ones; 5-9 -deposits of the Sylvitsa group: 5 -Ust-Sylvitsa formation, 6 -Chernyi Kamen formation, 7-9 -Staropechny and Perevalok formations: 7 -non dissected ones, 8 -Perevalok formation, 9 -Staropechny formation; 10 -Serebryanaya group deposits with the intersecting bodies of the Pre-Paleozoic intrusions, non dissected ones; 11 -deposits of the Basega group of the Upper Riphean; 12 -Post Early Carboniferous dikes of alkaline picrites; 13 -Late Devonian dikes of gabbro-dolerites; 14 -boundaries: a -tectonic, b -geological; 15: a -strike and dip of strata, b -position and numbers of localities of macrofossils. Localities of macrofossils: 1 -Shirokovskoe-1, 2 -Shirokovskoe-2, 3 -Usva-Vilukha, 4 -Usva-Krutikha, 6 -Koiva, 7 -Sylvitsa-1, 8 -Sylvitsa-2, 9 -Sylvitsa-3, 10 -Sylvitsa-4, 11 -Sylvitsa-5. ...
The publication represents the second part of the series «Upper Vendian macrofossils of Eastern Europe». Fossils of the Middle Urals (Sverdlovsk Region and Perm Territory) and the Southern Urals (Chelyabinsk Region and the Republic of Bashkortostan) are discussed in this report. As in the first part, it contains descriptions of genera and species of macrofossils mainly in early editions, images of typical specimens, information on their location and a place of storage. A significant section of the publication is an overview of the geological study of the Vendian of the region with a revision of the information about the localities of macrofossils.
