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Article

Late Cenozoic Uguumur and Bod-Uul Volcanic Centers in Northern Mongolia: Mineralogy, Geochemistry, and Magma Sources

by
Alexander Perepelov
1,*,
Mikhail Kuzmin
1,
Svetlana Tsypukova
1,
Yuri Shcherbakov
1,
Sergey Dril
1,
Alexey Didenko
2,
Enkhbat Dalai-Erdene
3,
Mikhail Puzankov
4 and
Alexander Zhgilev
1
1
Vinogradov Institute of Geochemistry, SB RAS, 664033 Irkutsk, Russia
2
Kosygin Institute of Tectonics and Geophysics, FEB RAS, 680000 Khabarovsk, Russia
3
Institute of Geology, Mongolian Academy of Sciences, Ulaanbaatar 13331, Mongolia
4
Institute of Volcanology and Seismology, FEB RAS, 683006 Petropavlovsk-Kamchatsky, Russia
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(7), 612; https://doi.org/10.3390/min10070612
Submission received: 2 June 2020 / Revised: 1 July 2020 / Accepted: 6 July 2020 / Published: 8 July 2020
(This article belongs to the Special Issue Mineralogical, Geochemical, and Isotope for Igneous Intrusions and Metamorphic Rocks of Siberian Craton)
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Abstract

:
The paper presents new data on mineralogy, geochemistry, and Sr-Nd-Pb isotope systematics of Late Cenozoic eruption products of Uguumur and Bod-Uul volcanoes in the Tesiingol field of Northern Mongolia, with implications for the magma generation conditions, magma sources, and geodynamic causes of volcanism. The lavas and pyroclastics of the two volcanic centers are composed of basanite, phonotephrite, basaltic trachyandesite, and trachyandesite, which enclose spinel and garnet peridotite and garnet-bearing pyroxenite xenoliths; megacrysts of Na-sanidine, Ca-Na pyroxene, ilmenite, and almandine-grossular-pyrope garnets; and carbonate phases. The rocks are enriched in LILE and HFSE, show strongly fractioned REE spectra, and are relatively depleted in U and Th. The low contents of U and Th in Late Cenozoic volcanics from Northern and Central Mongolia represent the composition of a magma source. The presence of carbonate phases in subliquidus minerals and mantle rocks indicates that carbon-bearing fluids were important agents in metasomatism of subcontinental lithospheric mantle. The silicate-carbonate melts were apparently released from eclogitizied slabs during the Paleo-Asian and Mongol-Okhotsk subduction. The parent alkali-basaltic magma may be derived as a result from partial melting of Grt-bearing pyroxenite or eclogite-like material or carobantized peridotite. The sources of alkali-basaltic magmas from the Northern and Central Mongolia plot different isotope trends corresponding to two different provinces. The isotope signatures of megacrysts are similar to those of studied volcanic centers rocks. The P-T conditions inferred for the crystallization of pyroxene and garnet megacrysts correspond to a depth range from the Grt-Sp phase transition to the lower crust. Late Cenozoic volcanism in Northern and Central Mongolia may be a response to stress propagation and gravity instability in the mantle associated with the India-Asia collision.

1. Introduction

Alkali-basaltic volcanism in the Baikal-Mongolia province south of the Siberian craton erupted for more than 30 myr from the Oligocene to the Holocene. Multiple events of magmatic activity have produced geographically dispersed volcanic fields (Figure 1a), sometimes of controversial origin. Volcanism in the region has received ample literature [1,2,3,4,5,6,7,8,9,10,11,12,13,14,15,16,17].
The available publications discuss Late Cenozoic volcanism in terms of ages, mineralogy, major- and trace-element chemistry, and isotope systematics used to reconstruct the sources of magma and causes of Late Cenozoic volcanic activity in Central Asia. Several models explain the petrogenesis of within-plate alkali-basaltic magmas in Central Asia in the context of (i) passive or active rifting; (ii) mantle plume activity or sublithospheric mantle upwelling [7,9,14]; (iii) recycling of slabs from past subduction events [19]. With new field data from volcanic fields in Mongolia collected in 2006 through 2019, we expect to shed more light on Late Cenozoic magmatism in Central Asia.
Samples of erupted material can provide evidence for the sources and formation conditions of alkali-basaltic magmas in intracontinental provinces. Sites of explosive eruptions exist in Central Mongolia [7,9] and in a few fields of southern Siberia, Russia: Areas of Lake Baikal, Vitim Plateau, and Udokan Range. The evolution of an eruptive center shows up in geomorphically expressed lava cones, volcanic pipe structures, or lava-pyrocalstic flows and subvolcanic bodies associated with fracture systems that act as magma conduits. The products of explosive eruptions often carry peridotitic, pyroxenitic, and granulitic mantle or crustal xenoliths, megacrysts of leucocratic or melanocratic minerals, as well as traces of carbon-bearing fluids that were involved into the evolution of the magmatic system. Data on diverse eruption products have implications for magma sources, conditions of within-plate magma generation, as well as for the structure and composition of lithospheric and asthenospheric mantle.
We have studied the Uguumur and Bod-Uul volcanic centers in Northern Mongolia (Figure 1b). The obtained mineralogical and isotope-geochemical results make basis for a petrological-geodynamic model and provide insights into the causes of Late Cenozoic within-plate magmatic activity in Central Asia. The modeling has been done with reference to the known geodynamic history of the Central-Asian Orogenic Belt (CAOB) bordering the Siberian craton in the south.

2. Geological Background. Uguumur and Bod-Uul Volcanic Centers

The Late Cenozoic Uguumur and Bod-Uul volcanic centers (Figure 1b) originated within the Tesiingol volcanic field in Northern Mongolia in the Middle to Late Miocene and have 40Ar/39Ar ages between 13 and 8 Ma [14].

2.1. Uguumur Volcano

We named the volcano Uguumur after the local name of a nearby Uguumur mountain (2329 m asl). The volcano is located on the eastern margin of a large Late Cenozoic lava plateau in the upper reaches of the Agaryn-gol in Hovsgol aimak, Mongolia (Figure 1b). It looks like a heavily eroded edifice, of a moderate volume and an ordinary shape, poorly expressed in the surface topography; it is up to 1.5 km in diameter (Figure 2a) and has a deformed water-filled crater, 150 m in diameter, at the center. The volcano is composed of voluminous pyroclastic material and scarce <4 m thick lava flows, about 14 m of total thickness, with mainly explosive breccia and scoria in the northern and eastern sectors. The volcano formed upon a Lower Paleozoic limestone, phosphorite, quartzite, and meta-sandstone basement which was mobilized during volcanism.
The Uguumur lavas and pyroclastics are of basaltic trachyandesite or less often trachyandesitic compositions and enclose numerous peridotitic (<10–12 cm) and few garnet-pyroxenite (2 to 20 cm) xenoliths and abundant megacrysts. The megacrysts are sanidine K-feldspar (~60–75%), pyroxene (~15–20%), ilmenite (2–3%), and garnet (<1%) reaching sizes of 4 × 9 cm (sanidines), 4 × 6 cm (pyroxenes and garnets), or 1 × 1 cm (ilmenites). Some breccias have unusual compositions and contain abundant megacrysts of ilmenite with a magmatic matrix and carbonate inclusions, as well as rare apatite megacrysts. Carbonate phases (Figure 3) are quite widespread in lava and breccia samples or appear as encrustation on clasts.
The Uguumur xenoliths and megacrysts are as diverse as in the Shavaryn-Tsaram volcanic center in the Tariat volcanic field of Central Mongolia [20,21].

2.2. Bod-Uul Volcano

Bod-Uul volcano (a local name of a mount) is located 3 km east of Lake Gashuun-nuur in Northern Mongolia (Figure 1b). It is heavily eroded, with many subvolcanic bodies exposed in its central part. The volcanic center rises up to ~50 m over Late Pleistocene-Holocene lacustrine deposits in a small basin (Figure 2b). The oval ~2.5 × 1.5 km edifice is elongate in the W–E direction. It has 2–3 m thick and ~0.5–1 km long remnant lava flows at the foot, a thick (up to 2 m) scoria layer on the eastern slope, and small broken craters in the southeastern and northeastern parts. Unlike Uguumur, the Bod-Uul rocks are basanite and phonotephrite. Its lavas, subvolcanic bodies, and scoria lack xenoliths and are free from signatures of crustal contamination, but contain abundant carbonate inclusions.

3. Analytical Procedures

Minerals were analyzed by scanning electron microscopy coupled with energy-dispersive spectrometry (SEM EDS) using a Carl Zeiss LEO-1430VP electron microscope equipped with an Oxford Instruments INCA Energy 350 analytical system, at the Geological Institute, Siberian Branch of the Russian Academy of Sciences in Ulan-Ude. The operating conditions were: 20 kV accelerating voltage, <0.5 nA beam current, 0.1 μm beam diameter, and 50 s counting time.
Major and trace elements were measured at the Share-Use Analytical Center for Isotope and Geochemical Studies (Vinogradov Institute of Geochemistry, Irkutsk, Russia). Major elements in rocks and minerals were determined by X-ray fluorescence (XRF) on a Bruker AXS S4 Pioneer wavelength dispersive X-ray fluorescence spectrometer (Bruker AXS, Karlsruhe, Germany), as in [22]. Trace elements were determined by inductively coupled plasma mass spectrometry (ICP-MS) on a ThermoFinnigan ELEMENT 2 double focusing magnetic sector field mass spectrometer (Finnigan MAT, GMBH, Bremen, Germany), as in [23]. The contents of FeO in rocks were analyzed as in [24]. The quality of trace elements analyses was checked against international USGS standards (BHVO-2, AGV-2) [25].
Sr and Nd isotopes in rocks and minerals were studied by extraction chromatography using EIChroM Industries II resins (Eichrom Technologies, 1955 University Lane, Lisle, Clarinda, IA, USA): TRU Spec and Ln Spec for total REE extraction and separation of Sm and Nd, and Sr Spec for Sr extraction, as in [26]. Pb was extracted with BioRad-AG1X8 resin (Bio-Red, Hercules, CA, USA), by a method slightly modified after [27]. Nd and Sr isotope ratios were analyzed on a Thermo Fisher Finnigan MAT-262 ion collector thermal ionization mass spectrometer (Finnigan MAT, GMBH, Bremen, Germany) at the Share-Use Analytical Center for Geodynamics and Geochronology (Institute of the Earth’s Crust, Irkutsk, Russia). The measurement of the Nd and Sr isotopic ratios was carried out by the Finnigan MAT 262 Thermal Ionization Mass Spectrometer (TIMS). The accuracy of the analysis was checked by measuring the SRM 987 (87Sr/86Sr = 0.710250 certified) and JNd-1 (143Nd/144Nd = 0.512100 certified) standards [28,29]. The values obtained in parallel experiments were: 0.710255 ± 15 (n = 19) for the SRM 987 and 0.512101 ± 6 (n = 34) for JNd-1. During mass spectrometric measurements, the isotope ratios were normalized to 88Sr/86Sr = 8.375209 and 146Nd/144Nd = 0.7219, respectively. Concentrations of Rb, Sr, Sm, Nd (ppm) were determined by the ICP-MS.
Lead isotope ratios were measured on a Fisheron Scientific GmbH NEPTUNE Plus ICP-MS multicollector mass spectrometer at the Share-Use Analytical Center for Isotope and Geochemical Studies (Vinogradov Institute of Geochemistry, Irkutsk, Russia), by double isotope dilution, using a mixed 207Pb–204Pb tracer; the tracer composition was optimized as recommended in [30,31]. The Pb concentration in the solution was 50–100 ng/mL. The spectra were corrected for 204Hg. The 208Pb background did not exceed 3 × 10−15A; 202Hg in the lead spectrum was 2 × 10−15A on average. The total ion current for 208Pb was at least 3 × 10−11A. Replicate measurements (n = 27) of the NIST SRM-981 standard [32] yielded ratio values of 206Pb/204Pb = 16.9376 ± 0.0022; 207Pb/204Pb = 15.4918 ± 0.0022; 208Pb/204Pb = 36.695 ± 0.006. The error was 2σ = 0.017–0.019%.

4. Mineralogy of Rocks, Megacrysts, and Xenoliths

4.1. Uguumur Volcano

The Uguumur basaltic trachyandesites and trachyandesites have fine porphyritic textures and share a similar mineralogy (Table 1): Mainly olivine (Ol), plagioclase (Pl), and clinopyroxene (Cpx) phenocrysts and subphenocrysts, with 5 to 15 μm Fe-Cr spinel inclusions in olivine cores and rims. Olivine crystallized in a Fo76-36 range, in a sequence from phenocrysts to subphenocrysts and microlites; the Ol + Cpx + Pl + Kfs + TiMgt + Ilm + Ap microlite assemblage formed at the final stage.
The Uguumur lava and pyroclastic samples bear calcitic and dolomitic carbonate phases (Table 1). The calcitic phases occur in most of basaltic trachyandesite breccias as numerous isometric 500–700 µm inclusions with distinct boundaries (Figure 3). They quite often enclose 5 to 80 µm crystals of hydroxy- and fluorapatite, sometimes containing up to 0.8 wt% SrO. The dolomitic carbonates were found in basaltic trachyandesite lavas as uniformly distributed interstitial inclusions between feldspar microlites. The inclusions range in size from few µm to ~500 µm and have prominent concentric zoning according to CaO and MgO variations.
Megacrysts in the Uguumur lavas and pyroclastics are of Na-sanidine (An3–4 Ab44–51 Or45–52), Ca-Na pyroxene with omphacitic compositions (Di70–77 Jd19–28 Ae0–8), ilmenite (TiO2 46–52 wt%, MgO 1.0–1.7 wt%), and almandine-grossular-pyrope garnet (Alm60–66 Grs17–20 Pyr14–17) compositions (Table 2). Many sanidine megacrysts are homogeneous in the core and have quasi-parallel tubular voids, up to 1–3 cm long and 0.1 to 2–4 mm in diameter, in the rims (Figure 4). Garnet megacrysts (Figure 5a) bear signatures of shearing and kelyphitization in the rims. They have very low Cr2O3 contents and show eclogite affinity (Figure 6) in the classification of [33]. Pyroxene megacrysts are often molten and enclose pyroxene-like glass with up to 5.8 wt% Na2O.
The Uguumur lavas contain xenogenic pyrope-almandine-grossular garnet crystals (Pyr71–81 Alm7–14 Grs9–13) with up to 2.44 wt% Cr2O3 (Table 2), which however are absent among peridotite xenoliths and megacrysts.
Peridotitic xenoliths are most often medium-grained spinel (Sp) or rarely garnet-spinel (Grt-Sp) lherzolites (Table 2). Some strongly sheared lherzolite xenoliths contain veinlets of Ol + Opx + Cpx + Pl + Kfs + TiMgt + Sp. Fo91–79 olivines in sheared lherzolite samples are often altered and contain magnetite streaks and inclusions of Fe-bearing calcite (with up to 3.8 wt% FeO). Undeformed olivines in lherzolite fall within a narrow Fo90–88 range with up to 0.62 wt% NiO. Pyroxenes in lherzolite are mainly Cr-bearing diopside (Cr2O3 to 1.2 wt%) and enstatite (Cr2O3 to 0.6 wt%). Peridotitic garnets have pyrope-almandine-grossular compositions (Pyr70–78 Alm12–20 Grs11–13), which are non-stoichiometric (Pyr76–95 Alm1–20 Grs2–4) in reaction rims.
Medium-size Grt-bearing pyroxenite (Wo47–49 En41–44 Fs8–9) xenoliths consist mainly of (Table 3) diopside and pyrope-almandine-grossular garnet (Pyr52–55 Alm29–32 Grs15–17). Some diopside and garnet crystals are intergrown with rutile and ilmenite. There are fine veins and zones of amphibole (Mg-hastingsite), bitownite (An68–79 Ab21–29 Or0–2), Al-spinel, and dolomite assemblages (Table 3).
Breccias with abundant ilmenite megacrysts contain Ol, Cpx, Pl, Kfs and Mgt microlites and rare Ol (Fo42–53) subphenocrysts (Figure 5b, Table 3), as well as sporadic apatite megacrysts and olivine xenocrysts from sheared peridotite xenoliths (Fo83–90). Some ilmenite megacrysts enclose apatite, magnetite, pyrite, and calcite; the latter occurs also as veinlets in ilmenite crystals or as inclusions in the breccia matrix.

4.2. Bod-Uul Volcano

The Bod-Uul basanites have porphyritic textures with olivine (Fo83–70) phenocrysts (Table 4). The phenocrysts enclose sporadic 2–4 µm Al-spinel grains and numerous particles of carbonate and zoned carbonate phases. The zoned carbonate inclusions have Mg- and P-bearing calcite cores, with 2–6 wt% MgO and 0.4–0.8 wt% P2O5, and Cu-bearing dolomite rims (CuO 0.9–1.3 wt%), as well as chlorite-smectite selvages (Figure 7). Basanites have a fine-grained foidic (according to EMPA) groundmass that encloses clinopyroxene (Wo45–48 En39–43 Fs9–15), titanomagnetite (13–19 wt% TiO2; 2.3–3.3 wt% MgO), ilmenite (51–54 wt% TiO2; 3.4–7.8 wt% MgO), apatite (1.6–2.0 wt% SrO; 0.6–0.8 wt% Cl, 3.2–3.9 wt% F), leucite (Ks74–78 Qtz22–23), and nepheline microlites, and glass with nepheline solid solution compositions (Ne81–86 Ks9–12 Qtz4–10).
The Bod-Uul phonotephrites are more strongly devitrified than basanites. They have porphyritic textures with olivine (Fo84–64) phenocrysts and subphenocrysts of leucite (Ks76–78 Qtz22–24), nepheline (Ne79–81 Ks10–12 Qtz8–11), and K-feldspar (Or53–63 Ab36–44 An2–3) (Table 4); olivine phenocrysts enclose Cr-spinel. Microlites in the phonotephrite groundmass are similar in mineralogy to those in basanites (Ol-Sp-Cpx-Pl-Kfs-TiMgt-Ilm-Ap-Lc-Ne) but contain more abundant alkaline aluminosilicates and plagioclase. Judging by the mineralogical dissimilarity, the Bod-Uul basanites and phonotephrites hardly belong to a single fractionation series.

5. Major- and Trace-Element Chemistry

5.1. Uguumur and Bod-Uul Lavas and Pyroclastics

The two volcanic centers differ notably in rock compositions (Table 5; Figure 8). The compositions of Uguumur lavas and pyroclastics are more silicic and moderately alkaline hypersthene-normative (Hy3–10) and low magnesian (Mg# as 100Mg/(Mg + Fe) = 51–56), while those of Bod-Uul are nepheline-normative (Ne7–11), highly magnesian (Mg# 62–69), and silica-undersaturated. The Uguumur and Bod-Uul rock compositions, with high silica and alkalis, respectively, are unusual and rare among the Late Cenozoic volcanic rocks of Mongolia (Figure 8).
The Uguumur basaltic trachyandesites and trachyandesites contain higher concentrations of Rb, Na, K, Sr, and P but lower Y and HREE than the average OIB compositions (Figure 9a). The more alkaline Bod-Uul basanites and phonotephtites show still greater LILE and HFSE enrichments relative to OIB (Figure 9b). Compared to OIB, the rocks of the two volcanic centers have more fractionated REE compositions (La/Yb = 21–41) and are relatively depleted in U and Th, especially the Uguumur basaltic trachyandesites and trachyandesites (see prominent lows in the curves of Figure 9). In general, the concentrations of many LILE and HFSE components decrease with increasing SiO2 from the Bod-Uul basanites and phonotephtites to the Uguumur basaltic trachyandesites and trachyandesites. The ratios of La/Yb and Sr/Y are decreasing (35–41 to 21–28 and 49–53 to 43–46, respectively) while Ba/Nb and Ga/Sc are increasing (7–9 to 11–16 and 1.5–1.7 to 1.7–2.2, respectively) in the same direction (Table 5). Note that the rocks of both volcanoes differ markedly from their counterparts in the Darkhat and Hovsgol volcanic fields located farther in the north, especially in higher concentrations of Rb, Ba, and K (Figure 9).

5.2. Uguumur Megacrysts

The Uguumur megacrysts and single crystals from lavas and pyroclastics were analyzed in numerous representative samples that could be successfully selected due to their abundance and large sizes. The available representative trace-element data for megacrysts from volcanics are still scarce even though the compositions of such megacrysts worldwide have been largely documented [37,38,39,40,41,42]. In this respect, new analytical evidence from the Uguumur megacrysts is valuable for petrogenetic modeling (Table 6; Figure 10, Supplementary File S1).
Sanidine, pyroxene, and garnet megacrysts show only minor compositional variations, including trace-element contents, and cannot be divided into mineral groups. Eight analyzed feldspar megacrysts have Na-sanidine compositions and very similar trace-element patterns, with low but reliably determined abundances of Ti, Fe, Mn, Mg, and P, possibly, nonstructural impurities. The megacrysts have high contents of Sr (~2100–2600) and Ba (~2000–2700 ppm) and relatively high Rb, Ga, Pb, and Eu (Eu/Eu* = 9–19) but low Th, U, HFSE, REE, and Y, at La/Yb~2–4 (Table 6; Figure 10, Supplementary File S1). High contents of Ba and Sr in feldspar megacrysts were previously reported from different volcanic provinces [37,40], but the causes of their accumulation and distribution in the mineral remain poorly understood. Preliminary EDS evidence of Ba and Sr distribution in sanidine reveals zones of BaO and SrO enrichment (up to 2 wt%).
Pyroxene megacrysts likewise share much compositional similarity. All eleven analyzed samples are of Ca-Na type, with high Al2O3 (~6.5–8.5 wt%) and Na2O (~2.6–3.4 wt%) contents but relatively low TiO2 (~1.1–1.5 wt%) (Supplementary File S1). Judging by their proximity to omphacite, they cannot be classified as augite of volcanics or diopside of peridotitic or pyroxenitic mantle xenoliths. Although bearing signatures of melting and breakdown upon interaction with magma, the pyroxene megacrysts remain similar in trace-element and especially REE patterns (Figure 10, Supplementary File S1). They all contain minor K and P impurities and show notable variance in Ba, Nb, and Ta, possibly, due to the presence of feldspar, apatite, and ilmenite inclusions.
Garnet megacrysts were analyzed in six more or less strongly kelyphitized samples of different sizes. Some garnets, with relatively high Rb, Ba, Th, U, Nb, Ta, Sr, P, and LREE (La, Ce, Pr) abundances (Figure 10, Supplementary File S1), contain kelyphite veinlets and may have been altered upon interaction with magma during the ascent. Garnets of another type belong to the same assemblage but are homogeneous and lack the composition features found in the former group. ICP-MS data confirm that all analyzed garnet megacrysts are almost free from Cr (<1 ppm) and show Ge, Y, and HREE enrichment. They contain quite low but analytically significant contents of Na, K, and P, which may likewise be due to interaction with melts.
The choice of ilmenite megacrysts samples was quite limited because of their small sizes (no more than 1 cm across) and occurrence in intergrowths with feldspar and pyroxene. Trace-element patterns analyzed in two ilmenite crystals (Figure 10, Supplementary File S1) show notable Nb and Ta enrichment, moderate contents of Zr and Hf, and relatively high concentrations of V, Co, Cu, and Zn, but quite low contents of many LILE: <1 ppm Cr, Ge, Rb, Y, Pb, Th, U, and REE and <10 ppm Li, Ga, Sc, Sr, Mo, Sn, Ba, etc. The data shortage leaves much uncertainty of whether the elements are incorporated into the ilmenite structure or occur as impurities. Note that ilmenite has more fractionated REE spectra than other minerals in the assemblage: La/Yb~7–12 against ~0.1–4.4, respectively.
Apatite, which appears to be another component of the megacryst assemblage at Uguumur, was found as ≤0.5 cm crystals in breccia samples that contain also ilmenite megacrysts. Apatite crystals may be prone to rapid breakdown on the surface or may remain hidden among pyroclastics because of small sizes. At the time being, their compositions can be characterized only from EDS data, which show high F (3.1–5.1 wt%) and Sr (to 0.8 wt%). Some apatites are enclosed in ilmenite megacrysts and, in their turn, bear calcite inclusions (Table 3).

5.3. Pyroxenite Xenolith

The trace-element chemistry of xenogenic material in the Uguumur lavas and pyroclastics was analyzed in a single sample of Grt-bearing pyroxenite. Pyroxenite has high concentrations of Ni and Cr, low Nb and Ta, and moderately low Zr, Hf, P and Ti. The REE spectra are characterized by moderate REE depletion, with La/Yb~2, and relative Pb and Sr enrichment (Figure 11).

6. Isotope Systematics

6.1. Sr, Nd, and Pb Isotope Variations in Lavas and Pyroclastics

In this study, the 87Sr/86Sr, 143Nd/144Nd, 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios have been analyzed in all types of volcanic rocks from the Uguumr and Bod-Uul centers (Table 7 and Table 8). The Sr and Nd ratios obtained for Uguumr and Bod-Uul fall within the field of Late Cenozoic volcanics of Mongolia having narrow ranges of 87Sr/86Sr ratios (~0.704–0.705) but notable variations of ɛNd from about +3 to −11 (Figure 12a, Table 7).
The 87Sr/86Sr and 143Nd/144Nd ratios for the Uguumur basaltic trachyandesite and trachyandesite samples correspond to the zone of lowest ɛNd(i) values from −7.8 to −9.9 and minor 87Sr/86Sr(i) variations of ~0.7046–0.7048 (Table 7). The Bod-Uul silica-undersaturated feldspar-bearing basanites and phonotephrites have slightly less radiogenic Sr and Nd isotope signatures: 87Sr/86Sr(i) of ~0.7045–0.7047 and ɛNd(i) of −4.9 to −7.7 (Table 7). These values are inconsistent with a contribution from an EMI-type source.
Unlike the similar 87Sr/86Sr and 143Nd/144Nd signatures in the Late Cenozoic volcanics of Central and Northern Mongolia, the lead isotope compositions for the two provinces plot two different trends in the 206Pb/204Pb–207Pb/204Pb diagram (Figure 13a). This dissimilarity was mentioned earlier by [14]. Another piece of evidence [9] was that volcanic samples from the northeastern South Hangayn province of Central Mongolia had 206Pb/204Pb and 207Pb/204Pb signatures corresponding to those of Northern Mongolian rocks. The 206Pb/204Pb and 207Pb/204Pb ratios of Central Mongolian volcanics lie between the PREMA and EMI mantle reservoirs, whereas those of Northern Mongolian samples trend from the PREMA-EMI most radiogenic compositions toward MORB-type depleted mantle (D-DMM) (Figure 13a).
The lead isotope composition of the Uguumur and Bod-Uul samples (206Pb/204Pb, 207Pb/204Pb, 208Pb/204Pb) (Table 5 and Table 6) matches the trend of Late Cenozoic rocks from Northern Mongolia, with the least radiogenic 207Pb/204Pb ratios (Figure 13a,b). Note that 207Pb/204Pb decrease toward the D-DMM reservoir at increasing SiO2 contents from basanite to trachyandesite.

6.2. Sr and Nd Isotope Variations in Megacrysts

The 87Sr/86Sr and 143Nd/144Nd ratios were measured in the Uguumur sanidine, pyroxene, and garnet megacrysts (Table 9; Figure 12c). The ɛNd(i) values for the megacrysts (from −6 to −12) are generally similar to those for the Uguumur lava and pyroclastic samples, but each mineral species has its own range of both isotope ratios. The 143Nd/144Nd signatures (approximate ɛNd(i) values) are most radiogenic in sanidine (−6.6 to −7.2), least radiogenic in pyroxene (−11.5 to −12.1), and intermediate in garnet (−8.3 to −8.9) megacrysts.
The 87Sr/86Sr(i) ranges differ markedly among different mineral types of megacrysts as a function of Sr contents, which show an inverse correlation such as the Nd ratios (Figure 12c and Figure 14). Sr-rich sanidine megacrysts (up to ~2600 ppm) have 87Sr/86Sr(i) ratios about 0.7046 which are typical of the Uguumur rocks. Pyroxenes, with Sr (~150–200 ppm), have slightly higher 87Sr/86Sr(i) values of ~0.7050–0.7053, while garnet megacrysts with low Sr (~2–20 ppm) have remarkably higher 87Sr/86Sr(i) ratios of ~0.7079–0.7081.

7. Discussion

The new data on mineralogy and trace-element chemistry of rocks and xenogenic material from the Uguumur and Bod-Uul volcanic centers in Northern Mongolia have implications for the conditions of magma generation. Further insights into the magma sources and causes of Late Cenozoic magmatism in the southern surroundings of the Siberian craton may be gained from the isotope systematics of the analyzed rock and megacryst samples, with reference to the known geodynamic history of the Central Asian Orogenic belt and Central Asia as a whole.

7.1. P-T Conditions of Magma Generation

The temperature and pressure conditions of magma generation at the Uguumur and Bod-Uul volcanic centers were constrained using empirical geothermometers and geobarometers. The calculation procedure consisted of two steps which focused on: (1) Compositions of parent melts equilibrated with the known compositions of subliquidus olivines according to KD Fe/Mg: Fo76 and Fo84 for the Uguumur and Bod-Uul samples, respectively, and on (2) pressures and temperatures during the formation of model parent melts for a hydrous system calculated using equations 15, 21, and 42 from [46]. The boundary conditions were KD Fe/Mg = 0.30 ± 11 for the olivine-melt system and 451 FeO/FeOtotal = 0.9. Due to the fact that real volatiles in the melts content is unknown, it is calculated with formula H2O = (Ce(ppm) × 200) × 103 (wt%) suggested for OIB in [47]. The equilibrium between subliquidus olivine (Fo76 and Fo84) and model melts of Uguumur and Bod-Uul volcanoes is attained at minor substraction of olivine (2–4%; 1–3%, respectively) according to [46].
The P-T conditions at the origin of the Uguumur magma are hard to constrain because of possible crustal contamination which may be responsible for the lack of Fo > 76 olivines in the derived basaltic trachyandesites and trachyandesites. However, according to our data the P-T conditions inferred for Fo76 crystallization (~1120–1170 °C, ~8–11 kbar) at the Uguumur volcanic center correspond to depths of 25–30 km, or the lower crust (Figure 14).
The formation conditions of the Bod-Uul basanite and phonotephrite magma in a hydrous system (H2O~2.5 wt%) fall within a P-T range of ~1270–1310 °C and ~17–21 kbar (Figure 15) corresponding to the lithospheric mantle at depths of ~50–65 km.
The trace-element signatures of the Uguumur and Bod-Uul rock samples, as well as the indicator ratios (La/Yb = 21–28 and 34–41, Sm/Yb = 6.1–7.3 and 7.8–9.0, Sr/Y = 40–46 and 4–54, Ga/Sc = 1.6–2.0 and 1.5–17, respectively), reveal high percentages of a residual garnet phase in the magma source. According to trace-element modeling, we suggest that the magmas of the two volcanoes may result from partial melting of Grt bearing pyroxenite or eclogite-like material (Figure 16). The melt fractions may be ~2–8% for the Uguumur basaltic trachyandesite magma (estimated tentatively because of crustal contamination) and ~1–5% for the Bod-Uul basanite and phonotephrite magma.

7.2. Formation Conditions of Megacrysts

The P-T conditions at the origin of garnet and pyroxene megacrysts (Figure 14) were estimated using trace-element thermometry of Grt-Cpx pairs [57] and Cpx and thermobarometry, with equations 32b, 32d of Putirka (2008) [46].
Pyroxene megacrysts crystallized at ~15 to 18 kbar and ~1170 to 1200 °C in dry and hydrous (H2O = 0 to 5 wt%) conditions [46]. Higher crystallization temperatures of ~1180–1230 °C were inferred for Grt-Cpx pairs of megacrysts from REE patterns [57], with reference to Cpx barometry [46]. The calculations were performed using Sm, Eu, Gd, Tb, Dy, Ho, Er and Y but exclusive of La, Ce, Pr and Nd, in order to ensure a stable correlation in the Grt-Cpx pairs, because garnets show considerable LREE variations.
The compositions of garnet and pyroxene megacrysts differ markedly in Mg-number: Mg# ~18 against ~40–45, respectively, and thus may vary at larger pressure and temperature ranges, in comparison with ranges on (Figure 13b).
As it was mentioned above, the sanidine megacrysts contain quasi-parallel tubular voids, which may arise when drops of liquid fall on crystal faces and locally impede mineral growth during rapid crystallization [58].

7.3. Carbonate Material and Crustal Contamination of Magma

The presence of carbonate phases in rock samples from the Uguumur and Bod-Uul volcanic centers indicates that the carbonate material contributed to melt evolution and metasomatism of the subcontinental lithospheric mantle (SCLM). These phases are found precipitated on the surface of eruption products, appear as inclusions in the rock matrix, in subliquidus minerals, and in ilmenite megacrysts from breccia samples (Figure 3 and Figure 7), or fill interstices between mineral grains in peridotitic xenoliths (Table 2 and Table 3).
Melts may have assimilated carbonates present in the metamorphic-sedimentary basement beneath the two volcanoes. Otherwise, calcite and dolomite in the matrix of the Uguumur rocks, as well as carbonate encrustation on the surfaces of rocks from both volcanoes, may be of sedimentary origin. To check the hypotheses, the composition of carbonate phases on the surface of the Bod-Uul breccia samples analyzed by ICP-MS was compared with the compositions of carbonate sediments from intracontinental volcanic fields [59]. The comparison showed much similarity in trace-element variations, with depletion in LILE and especially HFSE at Sr and Pb peaks (Figure 16).
The presence of carbonate inclusions in subliquidus minerals and mantle rocks is evidence that carbon-bearing fluids were significant agents in metasomatism of lithospheric mantle or that carbonates were present in the enriched magma source. Dolomite-calcite-silicate inclusions in Fo82–76 olivines from the Bod-Uul basanites record the presence of carbonate-silicate melts immiscible with alkali-basaltic magma in the mantle. Such melts may result from melting of carbonated mantle Grt-bearing pyroxenite or eclogite of SCLM.

7.4. Role of Lower Crust Material

The Uguumur and Bod-Uul samples lack fully crystallized inclusions that may represent crystalline crust, though such findings were reported from other volcanic centers of Mongolia. Namely, inclusions of crustal material in the Shavaryn-Tsaram lavas in Central Mongolia [1,2,14,60] are intermediate or more rarely mafic and high-silica granulites. The Shavaryn-Tsaram granulites have high Ba, K, Sr and relatively low Nb, Ta, Ti, and especially U and Th (Figure 10).
The contents of U and Th are low in most of Late Cenozoic volcanics from Northern and Central Mongolia, including those from the Bod-Uul and especially Uguumur centers (Figure 9). The U-Th depletion might indicate a lower crust contribution to the magma source or crustal contamination of melts. A simple model supporting possible granulite involvement into magma generation can be checked for the case of Uguumur and Bod-Uul volcanoes. Assuming that the Bod-Uul basanites are the most proximal to the source melt composition, the Uguumur basaltic trachyandesites would fit the model magma composition at a proportion of 60% granulite and 40% basanite (Figure 17), which appears unrealistic. Moreover, the Uguumur and Bod-Uul volcanics lack Pb enrichment unlike the model magma.
Granulite inclusions from older volcanic rocks of Central Mongolia show isotope signatures inconsistent with low-radiogenic source composition. Compared with Late Cenozoic volcanics (Figure 12 and Figure 13), they have higher 87Sr/86Sr ratios and moderate ɛNd values [2,14]. On the other hand, low-radiogenic signatures appear in isotope ratios of the Uguumur megacrysts.

7.5. Magma Sources. Geodynamics and Causes of Late Cenozoic Magmatic Activity

The sources of alkali-basaltic magmas in Northern and Central Mongolia differ in Sr–Nd trends dividing the territory into two isotope provinces (Figure 12, Figure 13 and Figure 18). Judging by the isotope evolution trend, the Uguumur and Bod-Uul magmas were originally generated from an old source consisting of eclogitic or pyroxenitic components, with involvement of SCLM carbonatized peridotite, according to the results of our trace elements modeling. The key role of such a magma source in Late Cenozoic volcanic fields of Central Mongolia was inferred previously in the model of [9]. According to the model [9], this source may be an ancient oceanic crust submerged in the mantle in the range of 2.9–2.5 billion years.
The formation model of the alkali-basaltic magmas reveals several stages in the history of the two volcanic centers. At an early stage, slab fragments detectable by seismic tomography [61,62,63,64] stacked near the mantle transition zone when oceanic lithosphere subducted beneath Central and Northern Mongolia during the closure of the Mongol-Okhotsk and Central Asian oceans. Then, after the subduction had been completed, the slabs underwent eclogitization and melting with separation of silicate-carbonate melts that acted as metasomatic agents. The ascending slab-derived silicate-carbonate melts interacted with peridotite of the lithospheric mantle, as it was shown, for example, in the model of Xue et al. [65], and caused SCLM metasomatism. The process produced zones of carbonated peridotite in the upper mantle which became new sources for alkali-basaltic magma [66]. The contributions of an eclogitic source and carbonated mantle to the alkali-basaltic melts can account for such features of volcanic rocks from Northern and Central Mongolia as HFSE enrichment along with low radiogenic Sr values and low contents of U and Th [66]. Oceanic lithosphere in slabs subject to eclogitization is known to lose PGE and radioactive elements and to acquire extremely low Rb/Sr ratios [67]. These signatures appear in the eclogitized slab-derived silicate-carbonate melts, as well as in the compositions of melts derived from carbonated SCLM peridotite. The presence of carbonate phases in subliquidus olivine from the Bod-Uul basanite, peridotite xenoliths, and pyroxenite (see above) provides evidence for the significant role of carbonate matter in SCLM rocks of the region. The carbonate component was ignored in previous studies of late Cenozoic volcanism in Mongolia, but it may be a key diagnostic feature tracing the sources of alkali-basaltic magmas.
Late Cenozoic volcanism in Central and Northern Mongolia apparently had multiple causes. The fields of Late Cenozoic volcanism in the region are located within the Central Asian Orogenic Belt (CAOB) composed of fold structures, terrains, and Precambrian basement blocks. The orogenic system borders, along deep faults, the Siberian and North China cratons in the north and south, respectively, and the Sikhote-Alin orogen in the east [68]. The CAOB marks the convergent margin of the Paleo-Asian ocean that opened in the late Proterozoic upon the breakup of Rodinia [69] and existed until the Mesozoic as part of the Central-Asian, Inner Mongolian, and Mongol-Okhotsk oceans.
Seismological, tomographic, and paleomagnetic data from Central Asia revealed slab remnants at depths from the asthenospheric mantle to the D″ layer by [64,70]. The slabs could form during the closure of the Paleoasian and Mongol-Okhotsk oceans in Central Asia [61,63,64].
On the other hand, Late Cenozoic volcanism in Central and Northern Mongolia may be a response to stress and instability and local melting in the metasomatized SCLM, as a result of the India-Eurasia collision [71]. The relation of within-plate volcanism in Central Asia with the collisional events was mentioned, for instance, by [17,19]. The India-Eurasia collision was a major event in the Cenozoic history of Asia. The convergence since 45 ± 5 Ma, which followed a transform setting, led to a rigid collision at the final stage about 30 ± 5 Ma [72]. That was approximately the time of volcanic activity in Central Asia, which produced numerous volcanoes and lava fields from the Late Eocene (~38–33 Ma) through the Late Pleistocene and Holocene [7]. The collisional stress and strain propagated toward the Siberian craton (Figure 18) and became blocked about 5 Ma [73]. The collision led to mountain growth, while the rotation of the Amur plate with respect to Eurasia was among the causes of rifting in the Baikal region [74].

8. Conclusions

New data on mineralogy, trace-element chemistry, and Sr, Nd, and Pb isotope variations in products of Late Cenozoic volcanism sampled at the Uguumur and Bod-Uul volcanic centers in the Tesiingol volcanic field of Northern Mongolia have implications for the magma generation conditions, magma sources, and geodynamic causes of Cenozoic volcanic activity.
The Uguumur basaltic trachyandesite and trachyandesite lavas and pyroclastics contain spinel- and garnet-peridotite and garnet-bearing pyroxenite xenoliths; megacrysts of Na-sanidine, Ca-Na pyroxene, ilmenite, and almandine-grossular-pyrope garnets; and carbonate phases. The Bod-Uul subvolcanic bodies are composed of basanite and phonotephrite, with inclusions of calcite and dolomite in subliquidus minerals.
The obtained P-T estimates for the crystallization of pyroxene and garnet megacrysts (15 to 18 kbar and ~1170 to 1230 °C) correspond to a depth range from the Grt-Sp transition to the lower crust. The P-T crystallization conditions at the Uguumur volcanic center correspond to depths of 25–30 km (~1120–1170 °C, ~8–11 kbar), or the lower crust. The formation conditions of the Bod-Uul basanite and phonotephrite magma in a hydrous system fall within a P-T range of ~1270–1310 °C and ~17–21 kbar corresponding to lithospheric mantle at depths of ~50–65 km.
The Uguumur and Bod-Uul rocks share similarity in LILE and HFSE enrichment, strongly fractionated REE spectra, and depletion in U and Th. The low contents of U and Th record features of a source, possibly, SCLM metasomatized under impact of silicate-carbonated melts released from eclogitizied old slab melting. The magma may result from partial melting of Grt-bearing pyroxenite or eclogite-like material with participation of carbonatized peridotite. The presence of carbonate phases in subliquidus minerals and mantle rocks prompts that carbon-bearing fluids were important agents in metasomatism of subcontinental lithospheric mantle.
The sources of alkali-basaltic magmas in Northern and Central Mongolia were different in Pb isotope characteristics. They plot different isotope trends and belong to two provinces. The isotope signatures of megacrysts are similar to those of Uguumur lava and breccia samples.
Late Cenozoic volcanism in Northern and Central Mongolia may be a response to stress propagation and instability in the mantle, associated with the India-Asia collision.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/10/7/612/s1, Supplementary file S1.xls; Supplementary file S2.xls.

Author Contributions

Conceptualization, A.P. and M.K.; methodology, A.P. and A.D.; validation, Y.S. and S.D.; data curation, S.T., M.P., E.D.-E., and A.Z.; original draft preparation, A.P.; writing—review and editing, Y.S. and S.T. All authors have read and agreed to the published version of the manuscript.

Funding

The study was carried out as part of a government assignment (topic ID 0350-2019-0007) and was supported by grants 20-05-00116 and 18-55-91049-Mong_omi from the Russian Foundation for Basic Research.

Acknowledgments

We wish to thank T. Perepelova (V.S. Sobolev Institute of Geology and Mineralogy, Novosibirsk) for aid in the manuscript preparation. The authors are very grateful to the anonymous reviewers for the great work of reviewing the article and the valuable comments and suggestions that contributed to a significant improvement in the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Location maps of Late Cenozoic volcanism in Central and Northern Mongolia (a) and Uguumur and Bod-Uul volcanic centers in Northern Mongolia (b). (a) Late Cenozoic volcanoes in volcanic fields and centers in Northern (brown stars) and Central (blue stars) Mongolia. Arabic numerals stand for volcanic fields names: 1 = Darkhat; 2 = Hovsgol; 3 = Moron; 4 = Tesiingol; 5 = Lower Orhon-Selenge; 6 = Hanuin-gol; 7 = Ugiy-nuur; 8 = Tariat; 9 = Vodorazdelny; 10 = Upper Orhon; 11 = Valley of Lakes; 12 = Gobi-Altay; 13 = Gurwan-Saihan; 14 = Gobi-Tien Shan, complemented after [9,18]. (b) Uguumur and Bod-Uul volcanic centers (brown stars) and lava fields (dark green).
Figure 1. Location maps of Late Cenozoic volcanism in Central and Northern Mongolia (a) and Uguumur and Bod-Uul volcanic centers in Northern Mongolia (b). (a) Late Cenozoic volcanoes in volcanic fields and centers in Northern (brown stars) and Central (blue stars) Mongolia. Arabic numerals stand for volcanic fields names: 1 = Darkhat; 2 = Hovsgol; 3 = Moron; 4 = Tesiingol; 5 = Lower Orhon-Selenge; 6 = Hanuin-gol; 7 = Ugiy-nuur; 8 = Tariat; 9 = Vodorazdelny; 10 = Upper Orhon; 11 = Valley of Lakes; 12 = Gobi-Altay; 13 = Gurwan-Saihan; 14 = Gobi-Tien Shan, complemented after [9,18]. (b) Uguumur and Bod-Uul volcanic centers (brown stars) and lava fields (dark green).
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Figure 2. Field photographs of Uguumur (a) and Bod-Uul (b) volcanic centers. See the text for details of sizes and shapes.
Figure 2. Field photographs of Uguumur (a) and Bod-Uul (b) volcanic centers. See the text for details of sizes and shapes.
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Figure 3. Carbonate phases in an Uguumur sample. BSE (backscatterd electrones) images. Mineral names are abbreviated as Cc = calcite; Ap = apatite; Ol = olivine; Cpx = Ca-pyroxene; Pl = plagioclase; Fsp = K-Na feldspar; TiMgt = titanomagnetite. Carbonate phases commonly contain apatite microlites.
Figure 3. Carbonate phases in an Uguumur sample. BSE (backscatterd electrones) images. Mineral names are abbreviated as Cc = calcite; Ap = apatite; Ol = olivine; Cpx = Ca-pyroxene; Pl = plagioclase; Fsp = K-Na feldspar; TiMgt = titanomagnetite. Carbonate phases commonly contain apatite microlites.
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Figure 4. Sanidine megacrysts with tubular voids from Uguumur. See a homogeneous core and multiple voids aligned with crystal faces in the rim.
Figure 4. Sanidine megacrysts with tubular voids from Uguumur. See a homogeneous core and multiple voids aligned with crystal faces in the rim.
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Figure 5. Garnet megacrysts (a) and breccia with ilmenite megacrysts (b). See signatures of shearing and kelyphitization in garnet megacrysts and numerous ilmenites and lherzolite megacrysts in the magmatic matrix of breccia with a Pl-Cpx-Mgt microlite assemblage and inclusions of a calcitic phase (Cc).
Figure 5. Garnet megacrysts (a) and breccia with ilmenite megacrysts (b). See signatures of shearing and kelyphitization in garnet megacrysts and numerous ilmenites and lherzolite megacrysts in the magmatic matrix of breccia with a Pl-Cpx-Mgt microlite assemblage and inclusions of a calcitic phase (Cc).
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Figure 6. Cr2O3–CaO diagram for garnet megacrysts and garnets from mantle xenoliths and inclusions at Uguumur volcano [33]. Symbols are compositions of almandine-grossular garnet megacrysts (1), pyrope garnets from peridotitic xenoliths (2), pyrope garnets from reaction rims in peridotitic xenolithx (3), xenogenic pyrope garnets from lavas (4), xenogenic pyrope garnets from reaction rims in lavas (5), pyrope-almandine garnets from Grt-bearing pyroxenite xenolith (6), pyrope garnets from reaction rims in Grt-bearing pyroxenite (7). Garnets 3, 5, 7 are non-stoichiometric. Composition fields are after [29]: G0 = unclassified garnets; G1 = pyrope garnet megacrysts; G3 = eclogitic garnet; G4-G5 = pyroxenitic and websteritic low-Cr (G4) and high-Cr (G5) garnets (Mg# < 0.7); G9 = lherzolitic garnet (Mg# > 0.7); G10 = harzburgitic garnet; G12 = wehrlitic garnet.
Figure 6. Cr2O3–CaO diagram for garnet megacrysts and garnets from mantle xenoliths and inclusions at Uguumur volcano [33]. Symbols are compositions of almandine-grossular garnet megacrysts (1), pyrope garnets from peridotitic xenoliths (2), pyrope garnets from reaction rims in peridotitic xenolithx (3), xenogenic pyrope garnets from lavas (4), xenogenic pyrope garnets from reaction rims in lavas (5), pyrope-almandine garnets from Grt-bearing pyroxenite xenolith (6), pyrope garnets from reaction rims in Grt-bearing pyroxenite (7). Garnets 3, 5, 7 are non-stoichiometric. Composition fields are after [29]: G0 = unclassified garnets; G1 = pyrope garnet megacrysts; G3 = eclogitic garnet; G4-G5 = pyroxenitic and websteritic low-Cr (G4) and high-Cr (G5) garnets (Mg# < 0.7); G9 = lherzolitic garnet (Mg# > 0.7); G10 = harzburgitic garnet; G12 = wehrlitic garnet.
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Figure 7. Carbonate inclusions in olivines from Bod-Uul basanites. BSE images. BD-5100 is basanite; Fo82–78 = olivine phenocrysts; Cc, Dol = calcite and dolomite in carbonate inclusions from olivine; Chl = chlorite in rims around carbonate phase; Ilm = ilmenite; Ap = apatite.
Figure 7. Carbonate inclusions in olivines from Bod-Uul basanites. BSE images. BD-5100 is basanite; Fo82–78 = olivine phenocrysts; Cc, Dol = calcite and dolomite in carbonate inclusions from olivine; Chl = chlorite in rims around carbonate phase; Ilm = ilmenite; Ap = apatite.
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Figure 8. SiO2 vs (Na2O + K2O) diagram for Uguumur and Bod-Uul rocks [34]. Stars are compositions of Uguumur (brown) and Bod-Uul (blue) lavas and pyroclastics. Crosses are compositions of Late Cenozoic volcanics from Central and Northern Mongolia [1,2,3,4,6,7,8,9,10,11,12,14,17].
Figure 8. SiO2 vs (Na2O + K2O) diagram for Uguumur and Bod-Uul rocks [34]. Stars are compositions of Uguumur (brown) and Bod-Uul (blue) lavas and pyroclastics. Crosses are compositions of Late Cenozoic volcanics from Central and Northern Mongolia [1,2,3,4,6,7,8,9,10,11,12,14,17].
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Figure 9. Mantle-normalized trace-element patterns for Uguumur (a) and Bod-Uul (b) rocks. (a) Uguumur basaltic trachyandesites and trachyandesites (brown); (b) Bod-Uul basanites and phonotephrites (blue). Normalization values are from [35]. OIB is the average composition of oceanic island basalt [36]. n is the number of analyses. Compositions of volcanics from Northern Mongolia are after [3,10,12,14] and our data.
Figure 9. Mantle-normalized trace-element patterns for Uguumur (a) and Bod-Uul (b) rocks. (a) Uguumur basaltic trachyandesites and trachyandesites (brown); (b) Bod-Uul basanites and phonotephrites (blue). Normalization values are from [35]. OIB is the average composition of oceanic island basalt [36]. n is the number of analyses. Compositions of volcanics from Northern Mongolia are after [3,10,12,14] and our data.
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Figure 10. Chondrite-normalized REE (a) and mantle-normalized trace element (b) patterns for Uguumur megacrysts, average compositions. Compositions of megacrysts are as in Table 7 and Supplementary File S1. Normalization values are from [35] for chondrite (a) [36] for primitive mantle (b). Numerals in braces are numbers of analyses; thin vertical bars are intervals of element contents (ppm). Uguumur rock compositions (olive green) are according to Figure 9a.
Figure 10. Chondrite-normalized REE (a) and mantle-normalized trace element (b) patterns for Uguumur megacrysts, average compositions. Compositions of megacrysts are as in Table 7 and Supplementary File S1. Normalization values are from [35] for chondrite (a) [36] for primitive mantle (b). Numerals in braces are numbers of analyses; thin vertical bars are intervals of element contents (ppm). Uguumur rock compositions (olive green) are according to Figure 9a.
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Figure 11. Mantle-normalized trace-element patterns for granulite (Mongolia) and garnet-bearing pyroxenite (Uguumur) xenoliths. Average compositions are according to [14] for granulite inclusions in Shavaryn-Tsaram lavas, Central Mongolia. n is the number of analyses. Normalization values are from [35].
Figure 11. Mantle-normalized trace-element patterns for granulite (Mongolia) and garnet-bearing pyroxenite (Uguumur) xenoliths. Average compositions are according to [14] for granulite inclusions in Shavaryn-Tsaram lavas, Central Mongolia. n is the number of analyses. Normalization values are from [35].
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Figure 12. 87Sr/86Sr vs. 143Nd/144Nd variations for Central and Northern Mongolia (a), Uguumur and Bod-Uul rocks (b) and megacrysts (c). Isotope ratios of Late Mesozoic—Early Cenozoic volcanic rocks in Mongolia (brown solid line) are according to [7]. Trend (blue solid line) and field (black dash line) for Late Cenozoic volcanics of Central and Northern Mongolia are according to [1,2,3,4,6,7,8,9,11,12,14,17]. (a) Isotope data for Late Cenozoic volcanic rocks of Central (blue cross) and Northern Mongolia (brown cross). Isotope data are according to [43] for D-DMM, DMM, MORB, and OIB, and to [44] for PREMA, EMI, and EMII. MORB and OIB trends (black solid line) are according to [45]. Average isotope ratios in mantle and crustal xenoliths from Late Cenozoic volcanics of Central Mongolia are according to [21] for peridotites and to [2,14] for granulites (age corrected, 250 Ma). Isotope data for the Uguumur and Bod-Uul rocks (b) and megacrysts (c) are age corrected (8 Ma). The question mark means high 87Sr/86Sr ratios in garnet megacrysts (see text). Other symbols are as in Figure 8.
Figure 12. 87Sr/86Sr vs. 143Nd/144Nd variations for Central and Northern Mongolia (a), Uguumur and Bod-Uul rocks (b) and megacrysts (c). Isotope ratios of Late Mesozoic—Early Cenozoic volcanic rocks in Mongolia (brown solid line) are according to [7]. Trend (blue solid line) and field (black dash line) for Late Cenozoic volcanics of Central and Northern Mongolia are according to [1,2,3,4,6,7,8,9,11,12,14,17]. (a) Isotope data for Late Cenozoic volcanic rocks of Central (blue cross) and Northern Mongolia (brown cross). Isotope data are according to [43] for D-DMM, DMM, MORB, and OIB, and to [44] for PREMA, EMI, and EMII. MORB and OIB trends (black solid line) are according to [45]. Average isotope ratios in mantle and crustal xenoliths from Late Cenozoic volcanics of Central Mongolia are according to [21] for peridotites and to [2,14] for granulites (age corrected, 250 Ma). Isotope data for the Uguumur and Bod-Uul rocks (b) and megacrysts (c) are age corrected (8 Ma). The question mark means high 87Sr/86Sr ratios in garnet megacrysts (see text). Other symbols are as in Figure 8.
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Figure 13. 206Pb/204Pb vs. 207Pb/204Pb variations for Central and Northern Mongolia (a), Uguumur and Bod-Uul rocks (b). Trend (blue solid line) and field (black dash line) for Late Cenozoic volcanics of Central and Northern Mongolia are according to [2,7,9,11,12,14]. Other symbols are as in Figure 8 and Figure 12.
Figure 13. 206Pb/204Pb vs. 207Pb/204Pb variations for Central and Northern Mongolia (a), Uguumur and Bod-Uul rocks (b). Trend (blue solid line) and field (black dash line) for Late Cenozoic volcanics of Central and Northern Mongolia are according to [2,7,9,11,12,14]. Other symbols are as in Figure 8 and Figure 12.
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Figure 14. P-T conditions of magma generation for Uguumur and Bod-Uul alkali basalts and megacrysts. Temperatures (°C) and pressures (kbar) are calculated using equations 15, 21, and 42 from [46]. Light blue field (Grt-Cpx megacrysts) corresponds to formation conditions of Uguumur megacrysts; n is number of Grt-Cpx pairs used for thermometry (see text for details). Geotherm and Sp-Grt phase transition lines for lithospheric mantle of Northern Mongolia are according to data from adjacent East Sayan area [48]. GrtPr and SpPr are depth facies domains of garnet and spinel peridotite. Dry solidus lines are after [49] for peridotite and [50] for Grt-pyroxenite. Magma generation depths are estimated assuming inferred pressures, average crust thickness of 45 km in the Baikal rift system [51], and crust and mantle densities of 2.9 and 3.3 g/cm3, respectively. Other symbols are as in Figure 8.
Figure 14. P-T conditions of magma generation for Uguumur and Bod-Uul alkali basalts and megacrysts. Temperatures (°C) and pressures (kbar) are calculated using equations 15, 21, and 42 from [46]. Light blue field (Grt-Cpx megacrysts) corresponds to formation conditions of Uguumur megacrysts; n is number of Grt-Cpx pairs used for thermometry (see text for details). Geotherm and Sp-Grt phase transition lines for lithospheric mantle of Northern Mongolia are according to data from adjacent East Sayan area [48]. GrtPr and SpPr are depth facies domains of garnet and spinel peridotite. Dry solidus lines are after [49] for peridotite and [50] for Grt-pyroxenite. Magma generation depths are estimated assuming inferred pressures, average crust thickness of 45 km in the Baikal rift system [51], and crust and mantle densities of 2.9 and 3.3 g/cm3, respectively. Other symbols are as in Figure 8.
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Figure 15. La/Yb-Sm/Yb (a,b) and Ga/Sc-TiO2 (c) trace-element modeling for generation of Uguumur and Bod-Uul alkali-basaltic magma. Magma generation models simulate equilibrium melting conditions for Grt-bearing pyroxenite (a) and eclogitic MORB (b,c) compared to garnet peridotite (depleted mantle). Element contents are in ppm. MORB composition is after [52]. Peridotite and Grt-pyroxenite compositions are from this study. Peridotite: 0.70 ppm La, 0.44 ppm Sm, 0.56 ppm Yb, 2.4 ppm Ga, 11.9 ppm Sc, and 0.14 wt% TiO2 (lherzolite inclusion in basanite of Tumusun volcano, Khamar-Daban Range, Russia); Grt-pyroxenite: 3.35 ppm La, 2.57 ppm Sm, 1.74 ppm Yb, 13.33 ppm Ga, 46.45 ppm Sc, 0.70 wt% TiO2 (pyroxenite inclusion in samples from Uguumur volcano). Mineral/melt partitioning is after published data [53,54,55,56]. Relative percentages of minerals are 60% Cpx and 40% Grt for eclogitic MORB and 80% Ol, 16% Cpx, and 4% Grt for garnet peridotite. Partial melting degrees are shown to vary within 0.5% to 10% for peridotite, 0.5% to 25% for eclogitic MORB, and 0.5% to 40% for Grt-pyroxenite. Variations of melting degrees are also shown for fertile peridotite mantle with different Cpx/Grt ratios (1.5–5.0). Symbols for Uguumur compositions are as in Figure 8.
Figure 15. La/Yb-Sm/Yb (a,b) and Ga/Sc-TiO2 (c) trace-element modeling for generation of Uguumur and Bod-Uul alkali-basaltic magma. Magma generation models simulate equilibrium melting conditions for Grt-bearing pyroxenite (a) and eclogitic MORB (b,c) compared to garnet peridotite (depleted mantle). Element contents are in ppm. MORB composition is after [52]. Peridotite and Grt-pyroxenite compositions are from this study. Peridotite: 0.70 ppm La, 0.44 ppm Sm, 0.56 ppm Yb, 2.4 ppm Ga, 11.9 ppm Sc, and 0.14 wt% TiO2 (lherzolite inclusion in basanite of Tumusun volcano, Khamar-Daban Range, Russia); Grt-pyroxenite: 3.35 ppm La, 2.57 ppm Sm, 1.74 ppm Yb, 13.33 ppm Ga, 46.45 ppm Sc, 0.70 wt% TiO2 (pyroxenite inclusion in samples from Uguumur volcano). Mineral/melt partitioning is after published data [53,54,55,56]. Relative percentages of minerals are 60% Cpx and 40% Grt for eclogitic MORB and 80% Ol, 16% Cpx, and 4% Grt for garnet peridotite. Partial melting degrees are shown to vary within 0.5% to 10% for peridotite, 0.5% to 25% for eclogitic MORB, and 0.5% to 40% for Grt-pyroxenite. Variations of melting degrees are also shown for fertile peridotite mantle with different Cpx/Grt ratios (1.5–5.0). Symbols for Uguumur compositions are as in Figure 8.
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Figure 16. Mantle-normalized trace-element patterns for carbonate phases from surfaces of Bod-Uul volcanics and carbonate sediments of French Massif Central after [59]. Normalization values are from [36].
Figure 16. Mantle-normalized trace-element patterns for carbonate phases from surfaces of Bod-Uul volcanics and carbonate sediments of French Massif Central after [59]. Normalization values are from [36].
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Figure 17. Mantle-normalized trace-element patterns for Uguumur model basaltic trachyandesite compositions, two-component mixing. Model composition is calculated assuming mixing of Bod-Uul basanite and phonotephrite magma (40%) and lower crust granulite from Mongolia (60%). n is the number of analyses Normalization values are from [36].
Figure 17. Mantle-normalized trace-element patterns for Uguumur model basaltic trachyandesite compositions, two-component mixing. Model composition is calculated assuming mixing of Bod-Uul basanite and phonotephrite magma (40%) and lower crust granulite from Mongolia (60%). n is the number of analyses Normalization values are from [36].
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Figure 18. Isotope provinces of Late Cenozoic volcanism in Central and Northern Mongolia. Dash and dotted lines are national border and coordinate grid, respectively. Brown squares and yellow triangles are lead isotope compositions (207Pb/204Pb–206Pb/204Pb) of Late Cenozoic volcanic fields of Northern and Central Mongolia. These geographical provinces respond to the different lines of Pb isotopic evolution as shown in Figure 13a. Brown stars—location of Uguumur and Bod-Uul volcanoes. Bolnayn fault is after [75]. Heavy dash lines are tentative boundaries of isotope provinces. Arrows show inferred direction of stress propagation from the India-Eurasia collision front. Numbers in boxes are age intervals of volcanism (Ma) for different fields according to the published evidence [2,3,9,18].
Figure 18. Isotope provinces of Late Cenozoic volcanism in Central and Northern Mongolia. Dash and dotted lines are national border and coordinate grid, respectively. Brown squares and yellow triangles are lead isotope compositions (207Pb/204Pb–206Pb/204Pb) of Late Cenozoic volcanic fields of Northern and Central Mongolia. These geographical provinces respond to the different lines of Pb isotopic evolution as shown in Figure 13a. Brown stars—location of Uguumur and Bod-Uul volcanoes. Bolnayn fault is after [75]. Heavy dash lines are tentative boundaries of isotope provinces. Arrows show inferred direction of stress propagation from the India-Eurasia collision front. Numbers in boxes are age intervals of volcanism (Ma) for different fields according to the published evidence [2,3,9,18].
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Table
Table 1. Average major-element compositions (wt%) of minerals from Uguumur volcanic rocks.
Table 1. Average major-element compositions (wt%) of minerals from Uguumur volcanic rocks.
MineralOlCpxPlPl*KfsSpTiMgtIlmApCcTiMgt*Ap*DolGM
Number of Analysis554734769946145
PhasesPhcrPhcrMcrMcrMcrInc*McrMcrMcr*Int*Int*Int*IntSEM
SiO238.2351.1555.7560.6264.72 56.79
TiO2 1.57 7.0224.7652.77 32.93 1.52
Al2O3 2.1826.0923.3319.829.451.57 1.172.64 17.62
Cr2O3 0.08 22.413.19
Fe2O3 1.430.240.190.6721.0515.533.39 2.50
FeO23.297.450.490.380.0033.4650.7740.680.70 58.570.590.263.55
MnO0.17 0.160.440.66 0.61 0.59
MgO38.4614.85 3.231.813.53 0.310.56 18.300.93
CaO0.1721.299.265.481.42 53.9554.45 54.3833.114.41
Na2O 0.265.727.535.91 5.17
K2O 0.520.947.22 5.06
P2O5 38.59 39.76 0.93
CO2 45.02 46.96
Total100.32100.2798.06 99.7696.7998.06101.0293.24100.5697.8194.7399.2195.97
End-members74.5 FoWo 43.6An 51.2An 67.4An 6.9Usp 19.1Usp 64.6Ilm 87.7 Cc 99.2Usp 92.8 Cc 55.9
25.3 FaEn 42.4Ab 45.8Ab 27.1Ab 51.6Sp 17.5Sp 9.4Gkl 11.1 Mgs 0.8Sp 3.1 Mgs 43.0
0.2 TfFs 14.0Or 3.0Or 5.5Or 41.5Mgt 28.5Mgt 20.4Prf 1.2 Sdr 0.0Mgt 1.4 Sdr 1.1
Chr 32.1Chr 4.4 Chr 0.0
Note: Number of analysis - shows the number of analyses of minerals used for averaging; letter superscripts are endmembers; Abbreviations stand for: Ol = olivine; Cpx = clinopyroxene; Pl = plagioclase; Kfs = K-Na feldspar; Sp = spinel; TiMgt = titanomagnetite; Ilm = ilmenite; Ap = apatite; Cc = calcite; Dol = dolomite; GM = groundmass; Phcr = phenocrysts; Mcr = microlites (Mcr* = average over GM microlites and inclusions in calcite phase; Inc* = inclusions (here in olivines); Int* = interstices (here carbonate phases and mineral inclusions in GM); Int = interstitial dolomite in GM; Fo = forsterite; Fa = fayalite; Tf = tephrite; Wo = wollastonite; En = enstatite; Fs = ferrosilite; An = anorthite; Ab = albite; Or = orthoclase; Ilm = ilmenite; Gkl = geikielite; Prf = pyrophanite; Cc = calcite; Mgs = magnesite; Sdr = siderite; Usp = ulvospinel; Sp = spinel; Mgt = magnetite; Chr = chromite. EMPA for groundmass: 500 × 1000 μm. Fe2O3/FeO, and CO2 are calculated according to stoichiometry. Average contents of other oxides and volatiles are: 0.27 wt% BaO in Pl*; 0.42 wt% BaO in Kfs; 0.85 wt% SrO; 4.10 wt% in F; and 0.20 wt% Cl in Ap; 0.80 wt% SrO; 3.60 wt% F; 0.17 wt% Cl; and 0.40 wt% SO3 in Ap*; 0.15 wt% ZnO; 0.35 wt% V2O3 in Sp; 0.63 wt% V2O3 in TiMgt; 0.28 wt% V2O3 in TiMgt*; 0.11 wt% V2O3 in Ilm.
Table
Table 2. Average major-element compositions (wt%) of minerals from Uguumur megacrysts, xenoliths, and inclusions.
Table 2. Average major-element compositions (wt%) of minerals from Uguumur megacrysts, xenoliths, and inclusions.
RockMegacrystsPeridotitic Xenoliths and Inclusions
MineralCpxKfsGrtIlmOlOpxCpxGrtGrt*Grt**SpSp*Sp**Cc*
Number of Analysis10862782119426334
SiO248.9865.3639.33 40.9655.5152.1542.3142.6442.06
TiO21.310.04*0.4649.53 0.550.020.000.24 0.230.23
Al2O37.7719.4119.030.58 3.275.6422.8020.7922.0056.1348.4343.87
Cr2O3<0.001* <0.001* 0.270.800.951.232.099.6816.7122.98
Fe2O30.98 0.005.77 0.151.651.516.230.832.233.853.52
FeO15.200.24*27.5041.8210.457.391.397.002.896.389.479.9213.133.41
MnO0.14 0.510.17 0.170.030.440.430.18 0.150.170.11
MgO6.50 3.701.0548.5332.4315.5220.6025.6320.6219.9318.9317.010.59
CaO14.650.696.340.16 0.6020.895.021.565.62 50.18
Na2O2.975.490.28* 1.50
K2O0.10*7.880.12*
NiO0.002* 0.001* 0.53 0.280.360.16
CO2 45.63
Total98.6099.1197.2799.09100.4799.79100.12100.66101.39100.0098.0298.57101.0799.92
End-membersAeg 3.4An 3.4Pyr 14.8Ilm 95.8 Fo 89.2Wo 1.2Wo 46.7Pyr 72.6Pyr 89.8Pyr 72.8Usp 0.0Usp 0.5Usp 0.5Cc 93.4
Jd 23.4Ab 49.7Alm 61.9Gkl 3.8Fa 10.8En 87.2En 48.2Alm 13.8Alm 5.4Alm 12.6Sp 78.3Sp 76.8Sp 69.6Mgs 1.5
Di 73.2Or 46.9Grs 18.3Prf 0.4Tf 0.0Fs 11.6Fs 5.1Grs 11.9Grs 3.2Grs 13.0Mgt 2.8Mgt 3.9Mgt 3.6Sdr 5.1
Chr 10.1Chr 18.0Chr 24.9
Note: Abbreviations stand for: Grt = garnet; Opx = orthopyroxene; Grt* = garnet in reaction rims from peridotite; Grt** = garnet xenolith; Sp = spinel in Sp-peridotite; Sp* = spinel in Grt-Sp peridotite; Sp** = fine-grained interstitial spinel; Cc* = interstitial calcite in reaction rims; Pyr = pyrope, Alm = almandine; Grs = grossular. Ol, Opx, Cpx, Grt, Sp are main phases in peridotite inclusions. *—are contents according to inductively coupled plasma mass spectrometry (ICP-MS). Other abbreviations and superscripts are as in the Table 1.
Table
Table 3. Average major-element compositions (wt%) of minerals from Uguumur Grt-bearing pyroxenite xenolith and breccia.
Table 3. Average major-element compositions (wt%) of minerals from Uguumur Grt-bearing pyroxenite xenolith and breccia.
RockGrt-PyroxeniteBreccia
MineralCpxOpxGrtGrt*IlmSpAmphDolIlm*Ap*Cc*
Number of Analysis51622434181023
SiO250.3553.2740.7844.84 43.09
TiO20.89 52.990.581.91 51.16
Al2O36.032.7421.2513.570.2752.5612.66 0.15
Cr2O3 0.29 0.22 0.00
Fe2O31.650.091.174.493.3710.464.14 5.86
FeO3.5912.7513.8615.8433.3421.142.76 39.140.910.77
MnO0.000.000.260.880.930.38 0.21 0.18
MgO13.5928.3114.8020.037.5011.9816.9020.933.73 0.33
CaO21.520.386.160.92 11.6930.69 51.8651.84
Na2O1.21 2.46
K2O 1.31
P2O5 39.16
F 1.83 3.80
CO2 46.94 41.71
Total98.8397.8398.28100.5798.4097.3298.7598.55100.2595.7394.88
End-membersWo 48.5Wo 0.76Pyr 54.5Pyr 66.6Ilm 76.9Usp 1.2 Cc 51.3Ilm 86.6 Cc 95.0
En 42.6En 79.12Alm 28.7Alm 29.6Gkl 21.6Sp 50.4 Mgs 48.7Gkl 13.0 Mgs 1.6
Fs 8.9Fs 20.12Grs 15.7Grs 1.8Prf 1.5Mgt 11.1 Sdr 0.0Prf 0.4 Sdr 1.8
Sps 0.5Sps 1.7 Hrc 36.1 Rdn 1.5
Note: Abbreviations stand for: Amph = amphibole (Mg-hastingsite); Grt* = pyroxenite-hosted garnets in reaction rims; Ilm* = ilmenite megacryst; Ap* = apatite megacryst; Cc* = calcite inclusions and veinlets in ilmenite; Sps = spessartite; Hrc = hercynite; Rdn = rhodonite. End-member compositions are in apfu. Apatite also contains 0.70 wt% SrO. Other abbreviations and superscripts are as in Table 1 and Table 2.
Table
Table 4. Average major-element compositions (wt%) of minerals from Bod-Uul basanites and phonotephrites.
Table 4. Average major-element compositions (wt%) of minerals from Bod-Uul basanites and phonotephrites.
MineralOlOl*Kfs*Lc*Ne*Sp*Cpx**TiMgt**Ilm**Ap*CcCcDolChlGM
Number of Analysis6632591436254462
PhasesPhcrPhcrPhcrPhcrPhcrInc*McrMcrMcrMcr*Inc*Inc*Inc*Inc*SEM
SiO238.7938.9665.7054.8647.02 51.11 3.0535.248.28
TiO2 9.111.7420.0356.15 1.1913.713.27
Al2O3 19.0521.7829.664.742.030.670.38 15.24
Cr2O3 20.290.29 0.44
Fe2O30.840.530.480.57 26.373.3230.221.67
FeO16.7716.78 0.8738.064.5644.6335.41 0.410.941.3515.36.32
MnO0.340.41 0.550.320.630.65 0.421.590.380.33
MgO42.5242.63 1.6113.802.625.52 2.195.7120.4718.314.33
CaO0.240.240.71 22.18 53.9751.4944.2228.040.657.88
Na2O 5.66 16.60 1.09 7.24
K2O 9.0722.793.62 0.723.67
P2O5 41.440.720.54 1.71
NiO0.480.45
F 3.97
CO2 44.1944.6447.04
Total99.98100.01100.6699.9997.76100.73100.4398.80100.2299.3799.4297.64101.5284.2297.92
End-membersFo 81.2Fo 81.4An 3.3Ks 77.2Ks 11.5Usp 24.7Wo 46.9Usp 56.4Ilm 78.0 Cc 93.9Cc 83.6Cc 48.7
Fa 18.8Fa 18.5Ab 47.3Ne 0.0Ne 80.1Sp 8.6En 40.6Sp 14.6Gkl 20.6 Mgs 5.5Mgs 15.0Mgs 49.5
Tf 0.1Tf 0.1Or 49.4Fs 22.8Fs 8.4Mgt 36.3Fs 12.5Mgt 42.1Prf 1.4 Sdr 0.6Sdr 1.4Sdr 1.8
Chr 28.9 Chr 0.0
Note: Ol, Cc, and Chl are minerals in basanite (sample BD-5100); Ol*, Lc* (leucite), Ne* (nepheline), Sp*, and Ap* are minerals in phonotephrite (sample BD-5098); Cpx**, TiMgt**, and Ilm** are average contents for minerals in basanite and phonotephrite; GM = basanite groundmass; Inc* = inclusions in olivines; SEM of groundmass: 150 × 150 μm. Average contents of other oxides and volatiles: 0.45 wt% BaO in Kfs*; 0.61 wt% ZnO in Sp*; 0.64 wt% V2O3; 0.49 wt% V2O3 in TiMgt**; 0.92 wt% V2O3 in Ilm**; 0.30 wt% Cl in Ap*; 1.10 wt% CuO in Dol; 0.21 wt% Cl. Other abbreviations and subscripts are as in Table 1 and Table 2.
Table
Table 5. Average major- and trace-element compositions of Uguumur and Bod-Uul rock samples.
Table 5. Average major- and trace-element compositions of Uguumur and Bod-Uul rock samples.
VolcanoUguumurBod-UulVolcanoUguumurBod-Uul
RockBTATABSPTRocksBTATABSPT
Number of Analysis6367 6367
SiO2, wt%52.3155.3144.7946.99Y21232827
TiO22.562.652.963.02Zr250271347330
Al2O314.3615.4612.5913.18Nb5156122108
Fe2O34.692.974.434.06Mo1.41.43.12.5
FeO5.514.496.466.61Sn3.33.73.43.2
MnO0.120.080.150.14Cs0.540.280.860.84
MgO5.013.438.937.53Ba704656987955
CaO6.075.767.717.22La30.634.662.356.0
Na2O3.844.344.294.23Ce71.479.0134.4121.4
K2O3.583.973.984.05Pr9.8610.7917.2615.75
P2O50.830.891.591.48Nd41.845.071.064.2
LOI1.280.831.390.90Sm8.979.5714.0413.04
Total100.16100.1899.2799.42Eu2.552.754.013.68
Mg#54.352.566.362.8Gd7.057.5610.9010.21
HyN*, NeN4.1*8.9*16.311.8Tb0.951.011.381.29
Li, ppm12101211Dy4.785.046.606.30
Be2.271.963.272.99Ho0.810.861.081.04
Sc14131514Er1.871.992.442.33
V148125156150Tm0.240.250.290.28
Cr10885220174Yb1.321.391.641.61
Co34274438Lu0.180.190.220.22
Ni6148205159Hf5.756.217.527.23
Cu30315751Ta2.833.106.475.86
Zn135143143133W0.560.541.771.27
Ga24.824.823.423.9Tl0.080.110.060.07
Ge1.361.341.251.38Pb2.743.362.732.60
Rb65658175Th1.672.043.443.09
Sr941100614891340U0.450.361.050.91
Note: Abbreviations stand for: BTA = basaltic trachyandesite; TA = trachyandesite; BS = basanite; PT = phonotephrite. Superscripts show the number of analyses used for averaging. Mg-number is Mg# = Mg/(Mg + Fe2+) × 100, mol%. HyN*, NeN are normative hypersthene and nepheline contents, respectively (CIPW). LOI—Loss On Ignition. Full data on chemical compositions of Ugumuur and Bod-Uul rock samples are provided in Supplementary File S2.
Table
Table 6. Average major- and trace-element compositions of Uguumur megacrysts.
Table 6. Average major- and trace-element compositions of Uguumur megacrysts.
MegacrystsKfsCpxGrtIlmMegacrystsKfsCpxGrtIlm
Number Analysis81162 8362
SiO2, wt%65.3548.9837.41 Y0.4713.09132.960.90
TiO20.081.310.4749.53Zr2.0710934.09152
Al2O319.417.7720.490.58Nb0.190.930.86211
Fe2O30.250.982.805.77Mo0.020.110.126.50
FeO0.0015.2028.0941.82Sn0.252.210.353.64
MnO0.0020.140.610.17Cs0.160.070.190.01
MgO0.036.503.581.05Ba229938.946.17.39
CaO0.6814.656.820.16La1.235.131.440.77
Na2O5.492.970.220.03Ce1.7219.923.671.43
K2O7.880.140.150.01Pr0.153.980.730.18
P2O50.020.070.060.01Nd0.4922.606.100.75
Total99.1998.71100.7099.42Sm0.097.206.120.19
End-membersOr 46.9Di 73.19Alm 64.1Ilm 95.8Eu1.342.192.980.06
Ab 49.7Jd 23.39Grs 18.1Gkl 3.8Gd0.106.1714.930.24
An 3.4Ae 3.42Prp 14.6Prf 0.4Tb0.010.893.390.03
Li, ppm5.9713.61.071.43Dy0.084.1625.880.21
Be0.240.850.140.03Ho0.020.555.130.04
Sc0.2916.214.23.89Er0.050.9411.700.10
V1.5212433.8118Tm0.010.091.240.01
Cr0.200.750.472.35Yb0.050.455.630.11
Co0.3348.542.5103Lu0.010.050.570.01
Ni0.3012.94.1625.2Hf0.054.161.003.18
Cu1.937.395.61100Ta0.090.070.106.45
Zn3.28219145698W0.050.050.110.29
Ga21.026.116.310.6Tl0.070.030.040.01
Ge0.551.492.980.64Pb0.910.450.580.13
Rb60.41.82.80.5Th0.050.160.280.07
Sr23011979.175.24U0.020.060.080.04
Note: Abbreviations and superscripts are as in Table 1 and Table 5. See Supplementary File S1 for original data.
Table
Table 7. Sr and Nd isotope data for Uguumur and Bod-Uul rock samples.
Table 7. Sr and Nd isotope data for Uguumur and Bod-Uul rock samples.
Sample IDRbSr87Sr/86Sr2σ87Sr/86Sr(i)SmNd143Nd/144Nd2σ143Nd/144Nd(i)εNd(i)
Ugumuur volcano
BD-4935659220.7047520.704738.740.00.51213250.512125−9.80
BD-4936649190.7046840.704668.439.00.51212650.512119−9.92
BD-4939659620.7046220.704609.242.90.51223560.512228−7.79
BD-49387010430.7045730.7045510.449.20.51222960.512222−7.91
BD-509013210160.7049220.704889.344.10.51217290.512165−9.02
Bod-Uul volcano
BD-50977915260.7044720.7044514.171.30.51238560.512379−4.86
BD-50987513400.7046710.7046513.064.20.512266140.512260−7.18
BD-50998514300.7047110.7046913.969.30.51228990.512283−6.73
BD-51008215160.7044720.7044514.976.90.512241120.512235−7.66
Note:87Sr/86Sr and 143Nd/144Nd are measured isotopic ratios; 87Sr/86Sr(i) and 143Nd/144Nd(i) are age corrected values (assumed age 8 Ma); εNd values are calculated using 147Sm/144Nd = 0.1967 and 143Nd/144Nd = 0.512638 for the present day chondrite uniform reservoir (CHUR). All within-run errors of isotopic ratios (2σ) correspond to the last decimal of the quoted values. The contents of Rb, Sr, Sm, Nd, U, Th, and Pb are quoted in ppm. Uguumur samples: BD-4935, 4936, 4939 = basaltic trachyandesites; BD-4938 = trachyandesite; BD-5090 = basaltic trachyandesite (Tesiingol field). Bod-Uul samples: BD-5097, BD-5100 = basanites; BD-5098, BD-5099 = phonotephrites.
Table
Table 8. Pb isotope data for Uguumur and Bod-Uul rock samples.
Table 8. Pb isotope data for Uguumur and Bod-Uul rock samples.
Sample IDUThPb206Pb/204Pb2σ207Pb/204Pb2σ208Pb/204Pb2σ206Pb/204Pb(i)207Pb/204Pb(i)208Pb/204Pb(i)
Uguumur Volcano
BD-49350.551.722.3317.65831815.42311637.60814017.640115.422337.5894
BD-49360.551.632.3117.66161515.42131337.59673317.643315.420537.5788
BD-49390.281.952.9817.62791515.41721537.60463617.620715.416937.5880
BD-49380.362.163.4017.63601615.42561537.62633517.627915.425237.6102
BD-50900.642.122.9517.59971415.41871437.60843417.583015.417937.5902
Bod-Uul Volcano
BD-50971.123.883.3517.59971415.41871437.60843417.795915.459137.6734
BD-50980.913.092.6017.8217915.4603937.70282417.665415.437437.5700
BD-50991.003.342.8717.69251315.43871237.60013217.672015.438537.5997
BD-51001.003.322.7517.69891515.43971337.62933317.767915.457937.6415
Note:206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb are measured isotopic ratios; 206Pb/204Pb(i), 207Pb/204Pb(i), 208Pb/204Pb(i), and εNd (i) are age corrected values (assumed age 8 Ma). Sample ID are as in Table 7.
Table
Table 9. Sr and Nd isotope data for Uguumur megacryst samples.
Table 9. Sr and Nd isotope data for Uguumur megacryst samples.
Sample IDRbSr87Sr/86Sr2σ87Sr/86Sr(i)SmNd143Nd/144Nd2σ143Nd/144Nd(i)εNd(i)
UG-grt-14.822.20.7084510.708386.27.20.51219990.512172−8.89
UG-grt-2c3.519.20.7081110.708055.56.60.51222670.512199−8.35
UG-Fsp-662.125670.7046310.704610.110.570.512263200.512257−7.24
UG-Fsp-2158.721090.7046220.704610.201.000.51229580.512289−6.61
UG-Cpx-23.31920.7050920.705088.627.30.51201990.512009−12.07
UG-Cpx-81.72150.7053110.705317.122.80.51204870.512038−11.50
Note:87Sr/86Sr(i) and 143Nd/144Nd(i) are age corrected values (assumed age 8 Ma). The legend is as in Table 7. UG-grt—garnet megacrysts; Ugs-Gsp—sanidine megacrysts; UG-Cpx—pyroxene megacrysts.

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Perepelov, A.; Kuzmin, M.; Tsypukova, S.; Shcherbakov, Y.; Dril, S.; Didenko, A.; Dalai-Erdene, E.; Puzankov, M.; Zhgilev, A. Late Cenozoic Uguumur and Bod-Uul Volcanic Centers in Northern Mongolia: Mineralogy, Geochemistry, and Magma Sources. Minerals 2020, 10, 612. https://doi.org/10.3390/min10070612

AMA Style

Perepelov A, Kuzmin M, Tsypukova S, Shcherbakov Y, Dril S, Didenko A, Dalai-Erdene E, Puzankov M, Zhgilev A. Late Cenozoic Uguumur and Bod-Uul Volcanic Centers in Northern Mongolia: Mineralogy, Geochemistry, and Magma Sources. Minerals. 2020; 10(7):612. https://doi.org/10.3390/min10070612

Chicago/Turabian Style

Perepelov, Alexander, Mikhail Kuzmin, Svetlana Tsypukova, Yuri Shcherbakov, Sergey Dril, Alexey Didenko, Enkhbat Dalai-Erdene, Mikhail Puzankov, and Alexander Zhgilev. 2020. "Late Cenozoic Uguumur and Bod-Uul Volcanic Centers in Northern Mongolia: Mineralogy, Geochemistry, and Magma Sources" Minerals 10, no. 7: 612. https://doi.org/10.3390/min10070612

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