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In experimental rabbits, cysteine injected intravenously in a dose of 1000 mg/kg temporarily bound zinc in β cells and prevented the formation of chelate zinc complexes in response to subsequent injection of diabetogenic zinc-binding substances that induce cell destruction. Injection of cysteine to animals was associated with a sharply negative reaction to zinc in β cells, which attests to blockade of zinc ions. Injection of cysteine few minutes after dithizone and formation of zinc-dithizone complex was followed by displacement of dithizone from the complex and prevented the development of diabetes in most animals. The most plausible mechanism of preventive effect of cysteine is the formation of 2:1 zinc-cysteine complex in β cells with possible fixation of Zn atom between sulfur atoms from SH groups of two cysteine molecules.

The rocks of the Olkhon terrane experienced high-grade regional metamorphism reaching granulite facies. In addition to regional metamorphism, they were subjected to contact metamorphism and autometamorphism (mafic dikes). Three types of regional metamorphism have been distinguished. A terrane collage north of the Orso Zone revealed two stages of regional metamorphism: early-stage granulite metamorphism (Т = 750–900°С, Р = 8–9 kbar, around 500 Ma) and late-stage amphibolite and low–amphibolite facies (Т = 550–710°С, Р = 4–6 kbar, 460–470 Ma). The Orso microterrane separating the Krestovsky island-arc subterrane from a collage of other microterranes contains high-pressure mineral assemblages (up to 10 kbar), which are characterized by the presence of high-calcium garnet in metapelites. The Orso microterrane and Krestovsky subterrane are characterized by relatively high-pressure path of metamorphism. An extended zone of contact high-temperature metamorphism related to the emplacement of gabbro of the second phase of the Ustkrestovsky Complex has been mapped in the Krestovsky subterrane. The temperature of formation of two-pyroxene hornfels after metaporphyrites of the Birkhin volcanoplutonic association is estimated at 750–850°С. Beerbachites were formed by autometamorphism of subvolcanic mafic bodies, which compose the northern part of the Tazheran composite massif (syenite, Ne-syenite, subalkaline gabbro), dikes in the Birkhin gabbro massif, as well as dikes and separate blocks in marble melange. The temperature of autometamorphism during formation of beerbachites is estimated from two-pyroxene geothermometer as 700–1000°С.

This paper describes the 2020 release of the GEISA database (Gestion et Etude des Informations Spectroscopiques Atmosphériques: Management and Study of Atmospheric Spectroscopic Information), developed and maintained at LMD since 1974. GEISA is the reference database for several current or planned Thermal and Short-Wave InfraRed (TIR and SWIR) space missions IASI (Infrared Atmospheric Sounding Interferometer), IASI-NG (IASI New Generation), MicroCarb (Carbon Dioxide Monitoring Mission), Merlin (MEthane Remote sensing LIdar missioN). It is actually a compilation of three databases: the “line parameters database”, the “cross-section sub-database” and the “microphysical and optical properties of atmospheric aerosols sub-database”. The new edition concerns only the line parameters dataset, with significant updates and additions implemented using the best available spectroscopic data. The GEISA-2020 line parameters database involves 58 molecules (145 isotopic species) and contains 6,746,987 entries, in the spectral range from 10−6 to 35877 cm−1. In this version, 23 molecules have been updated (with 10 new isotopic species) and 6 new molecules have been added (HONO, COFCl, CH3F, CH3I, RuO4, H2C3H2 (isomer of C3H4)) corresponding to 15 isotopic species. The compilation can be accessed through the AERIS data and services center for the atmosphere website (https://geisa.aeris-data.fr/), with the development of a powerful graphical tool and convenient searching, filtering, and plotting of data using modern technologies (PostgreSQL database, REST API, VueJS, Plotly). Based on four examples (H2O, O3, O2 and SF6), this paper also shows how the LMD in house validation algorithm SPARTE (Spectroscopic Parameters And Radiative Transfer Evaluation) helps to evaluate, correct, reject or defer the input of new spectroscopic data into GEISA and this, thanks to iterations with researchers from different communities (spectroscopy, radiative transfer).

We provide the results of study of the extremely enriched in Y-REE carbonate-fluorine isolations from biotite-arfvedsonite granite of the Katugin rare metal deposit. New chemical data of isolations mineral phases - gagarinite-(Y), tveitite-(Y), fluocerite-(Ce), basnaesite, fluornatropyroclore, are delivered. Carbonate-fluoride globule in quartz of hosting granite gives possibility to estimate crystallization order. This finding might be the evidence of silicate-fluorine immiscibility suggested before for Y-REE segregations in the Katugin granites. Fluorine melt segregation took likely place at the magmatic stage of biotite-arfvedsonite granite formation. It causes host granite depletion with fluorine and redistribution of REE and Y in fluorine salt melt.

Geological and mineralogical data are reported on the manganese occurrences of the Olkhon terrane (Western Baikal region), which are localized in metadolerites of the Ustkrestovsky Complex, high-temperature mafic hornfels, granites, calcitic marbles and calciphyres, and occasionally are developed as separate veins in gneiss granites or small lenses in quartzites. Most of them are made up of high-temperature mineral assemblages (Opx + Cpx + Pl + Ilm ± Grt± Bt ± Amp), the main manganese carriers in which are ferrorhodonite (33–36 wt % MnO), orthopyroxene (6–12 wt % MnO), and ilmenite (3–16 wt % MnO). Obtained data are in conflict with traditional concepts that these rocks are gondites (manganese-rich metamorphosed sediments) or that manganese flux in carbonate sediments was related to the volcanic activity that occurred simultaneously with sedimentation at about 500 Ma. The diversity of manganese occurrences was produced by metasomatic processes that occurred almost simultaneously with regional metamorphism and emplacement of subalkaline mafic bodies during collisional tectonogenesis (about 470 Ma).

Geological and mineralogical data are reported on the manganese occurrences of the Olkhon terrane (Western Baikal region), which are localized in metadolerites of the Ustkrestovsky Complex, high-temperature mafic hornfels, granites, calcitic marbles and calciphyres, and occasionally are developed as separate veins in gneiss granites or small lenses in quartzites. Most of them are made up of high-temperature mineral assemblages (Opx + Cpx + Pl + Ilm ± Grt ± Bt ± Amp), the main manganese carriers in which are ferrorhodonite (33–36 wt % MnO), orthopyroxene (6–12 wt % MnO), and ilmenite (3–16 wt % MnO). Obtained data are in conflict with traditional concepts that these rocks are gondites (manganese-rich metamorphosed sediments) or that manganese flux in carbonate sediments was related to the volcanic activity that occurred simultaneously with sedimentation at about 500 Ma. The diversity of manganese occurrences was produced by metasomatic processes that occurred almost simultaneously with regional metamorphism and emplacement of subalkaline mafic bodies during collisional tectonogenesis (about 470 Ma).

The pump-probe technique for investigating vibrationally excited states via high resolution Raman spectroscopy was applied to CH methane isotopologue. The dipole transitions between A totally symmetric vibrational states are not active in IR spectra but these states can be efficiently studied using selective high resolution Raman spectroscopy. 80 vibration-rotation transitions, most of which belong to the 2ν– ν band have been assigned in the observed Raman spectra reported in this work. Including the Raman transitions in the simultaneous data fit improves the accuracy of the effective Hamiltonian and also rovibrational upper state levels of the ν, 2ν and 2ν (A) bands. A more accurate model of the ν vibration-rotation transitions improves the interpretation of the temperature dependence of Raman spectra involving the Pentad and Tetradecad polyads., Part of the research was performed at Institute of Monitoring of Climatic and Ecological Systems under contract of Russian Science Foundation (RSF), grant No. 19-77-10046. The research at the V.E. Zuev Institute of Atmospheric Optics was supported by the Ministry of Science and Higher Education of the Russian Federation (V.E. Zuev Institute of Atmospheric Optics of Siberian Branch of the Russian Academy of Sciences). The supports of the CNRS (France) in the frame of “Laboratoire International Associé SAMIA”, of IDRIS / CINES computer centers of France and of the ROMEO computer center Reims-Champagne-Ardenne are acknowledged. R.Z. Martínez, D. Paredes-Roibás and D. Bermejo acknowledge the funding received from Project FIS2017-84391-C2-1-P of Ministerio de Economía y Competitividad.

Dismembered ophiolites in the Early Paleozoic Olkhon terrane, a part of the Baikal collisional belt in the southern periphery of the Siberian craton, occur as fault-bounded blocks of ultramafic and mafic rocks from a few meters to hundreds of meters in size. The ultramafic rocks are mainly dunite&ndash, harzburgite peridotites with gradual transitions between the lithologies, as well as moderate amounts of enstatitite, wehrlite, and clinopyroxenite, but no lherzolite. Most peridotites have strongly depleted chemistry and a mineralogy corresponding to the harzburgite type usual for ophiolites of suprasubduction zones (SSZ). The mafic rocks are leuco- to melanocratic gabbros with different relative percentages of clinopyroxene, olivine, and plagioclase, which enclose thin layers and lenses of clinopyroxenite and anorthosite. They bear back-arc basin geochemical signatures, a setting inferred for the Neoproterozoic southern Siberian craton. The gabbroic rocks are of two geochemical groups, most of their trace-element patterns show Ta-Nb minimums and Sr maximums common to suprasubduction zone ophiolites. Judging by the Ol + Opx + Chl + Chr mineral assemblages, the Olkhon peridotites underwent low amphibolite and amphibolite regional metamorphism at 500&ndash, 650 &deg, C. The occurrence of the ultramafic and mafic bodies is consistent with formation in an accretionary wedge metamorphosed during a collisional orogeny. The mantle and crustal parts of the Olkhon ophiolite suite apparently were incorporated into the terrane during the frontal collision of perio-oceanic structures with the Siberian craton. Then, in a later oblique collision event, they became dismembered by strike-slip faulting into relatively small bodies and fault blocks exposed in the present erosional surface.

We studied the petrography, mineralogy, and geochemistry of the Paleoproterozoic (2.06 Ga) granites of the Katugin massif (Stanovoy suture zone), which hosts the combined rare-metal Katugin deposit. Three groups of granites were distinguished: (1) biotite (Bt) and biotite–riebeckite (Bt–Rbk) granites of the western block of the massif; (2) biotite–arfvedsonite (Bt–Arf) granites of the eastern block; and (3) arfvedsonite (Arf), aegirine–arfvedsonite (Aeg–Arf), and aegirine (Aeg) granites of the eastern block. The Bt and Bt–Rbk granites of the first group are mainly metaluminous and peraluminous rocks with rather high CaO contents and the minimum F contents among the granites described here. It was suggested that the granites of this group could be derived from a source dominated by crustal rocks with a small addition of mantle materials. These granites probably crystallized from a metaluminous–peraluminous melt with elevated CaO and moderate F contents. Melts of such compositions are least favorable for the crystallization of ore minerals. The Bt–Arf granites of the second group are mainly peralkaline and show high contents of CaO and Y and low contents of Na2O and F. A mixed mantle–crust source was proposed for the Bt–Arf granites. The initial melt of the Bt–Arf granites could have a peralkaline composition with elevated CaO content and moderate to high F content. The Arf, Aeg–Arf, and Aeg granites of the third group are enriched in ore mineral and were classified as peralkaline granites with very low CaO contents, elevated Na2O and F contents, and usually very high contents of Zr, Hf, Nb, and Ta. Based on the geochemical and isotopic data, it was supposed that the source of the granites of the third group could be derivatives of basaltic magmas produced in an OIB-type source with a minor addition of crustal material to the magma generation zone. It was suggested that the primary melt of this granite group could be a peralkaline CaO-poor and F-rich silicic melt, which is most favorable for the crystallization of ore minerals. Based on the analysis of the geochemical characteristics of the three granite groups and their relationships within the Katugin massif, a qualitative model of its formation was proposed. According to this model, the Bt and Bt–Rbk granites of the western block crystallized first, followed by the Bt–Arf granites of the eastern block and, eventually, the Arf, Aeg–Arf, and Aeg granites enriched in ore minerals.

Multiphase aluminofluoride segregations were registered in aegirine–amphibole granite from the Vostochnyi massif of the Katugin rare-metal deposit. Among them are fluorides (fluorite), Ca–Na–Mg fluoraluminates (weberite, cryolite, pachnolite–thomsenolite, prosopite, gearksutite, ralstonite, and others), and Ba fluoraluminates, which had not been observed previously in this massif. Four fluoraluminates with high concentrations of Ba were found in aluminofluoride segregations: usovite Ba2CaMgAl2F14, the most abundant phase, and three potentially new minerals (BaAlF4(OH), BaCa2AlF9, and BaCa4AlF13). The chemical composition of Ba phases and the results of their Raman spectroscopic study are reported.

The paper provides details of local geology and mineralogy of the Tazheran Massif, which was the sampling site of perovskite used as an external standard in perovskite U-Pb dating by sensitive high-resolution ion microprobe (SHRIMP) and laser ablation inductively-coupled plasma (LA&ndash, ICP&ndash, MS) mass spectrometry. The Tazheran Massif is a complex of igneous (mafic dikes, syenite, nepheline syenite), metamorphic (marble), and metasomatic (skarn, calc&ndash, silicate veins) rocks. Metasomatites are thin and restricted to the complex interior being absent from the margins. Perovskite has been studied at four sites of metasomatic rocks of three different types: forsterite&ndash, spinel calc&ndash, silicate veins in brucite marble (1), skarn at contacts between nepheline syenite and brucite marble (2), and skarn-related forsterite&ndash, spinel (Fo-Spl) calc&ndash, silicate veins (3). Pervoskite from Fo-Spl calc&ndash, silicate veins (type 1) is almost free from impurities (&lt, 1 wt.% in total: 0.06%&ndash, 0.4% REE2O3, 0.10%&ndash, 0.22% Nb2O5, &le, 0.1% ThO2). The U contents are from 0.1 to 1.9 wt.% UO2 and are relatively uniform in perovskites from the same vein but differ from vein to vein of this type. Perovskite from the contact skarn (type 2) contains 1.5 to 4.5 wt.% REE2O3 but is poor in other impurities. Perovskite grains from skarn-related Fo-Spl calc&ndash, silicate rocks (type 3) belong to two generations that differ in REE, Nb, Th, Fe, and Na concentrations. Early-generation perovskites occurs as compositionally homogeneous octahedral or cubic-octahedral crystals with contents of impurities higher than in other varieties (3.6 wt.% REE2O3, 1.6 wt.% Fe2O3, 1.3 wt.% Nb2O5, 0.7 wt.% ThO2, 0.6 wt.% UO2, and 0.6 wt.% Na2O) but the lowest is at the respective site. Late-generation varieties show highly variable impurity concentrations of 1.5 to 22.7 wt.% REE2O3, 0.4 to 8.4 wt.% Nb2O5, and 0.8 to 4.5% ThO2, while the perovskite component may be as low as 65%. In addition to the lueshite and loparite, components, they contain REEFeO3 and Th0.5TiO3 endmembers which have no natural analogs.

The Arbarastakh Neoproterozoic ultramafic carbonatite complex is located in the southwestern part of the Siberian Craton (Aldan Shield) and contains ore-bearing Zr–Nb (REE) carbonatites and phoscorites. Carbonatites are mainly represented by calcite and silicocarbonatite varieties. The primary minerals composing the carbonatites are calcite and dolomite, as well as phlogopite, clinopyroxene, fluorapatite, amphibole, fluorite, K-feldspar and feldspathoids. Olivine (forsterite), Ti-magnetite, apatite, phlogopite, calcite, dolomite and the minor spinel group minerals form the primary phoscorites. The ore-bearing Zr–Nb mineral assemblages of the phoscorites and carbonatites include accessory zircon, zirconolite, perovskite, pyrochlore and baddeleyite. The Ba–Sr–REE hydrothermal mineralisation consists of ancylite-(Ce), bastnaesite-(Ce) and burbankite, as well as barite-celestite, strontianite, barytocalcite, and rare Cu–Fe sulphides. The silicocarbonatites and carbonatites formed in multiple stages from a single alkaline Ca–Na–K–silicocarbonatite melt, while the phoscorites are products of differentiation of the carbonatitic melt and were crystallised from an Fe-rich phosphate–carbonate melt at temperatures of more than 720 °C. The silicate–phosphate–carbonate melts were responsible for the Zr–Nb mineralisation of the carbonatites at temperatures of more than 540–575 °C; the hydrothermal REE-bearing mineral assemblages crystallised from saline (60–70 wt%) carbonatitic fluids of Na–Ca–Mg–F–carbonate composition at a minimum temperature range of 350–300 °C. The Ca–Sr-carbonate as well as the Na–hydro–carbonate fluids were responsible for the Ba–Sr–REE mineralisation of the phoscorites at ~500–480 and 450–430 °C.

Stable isotope compositions are examined for brucite marble and Mg-skarn that occur in the southern part of the Tazheran massif, Olkhon region, Russia. Brucite marble exhibits a narrow range in δ18O of +23.3 to +26.2 ‰ and shows carbon isotope depletion of −1.9 to −4.4 ‰) as compared with the country dolomite isotope compositions (+2.0 to +2.4 ‰) which is explained by both decarbonation processes and participation of fluids depleted in 13C. The emplacement of brucite marble was accompanied by the formation of endo- and exoskarn at the contact between syenite and brucite marble. δ18O profiles across the contact show a typical decrease towards the syenite side interpreted as the result of fluid/rock interaction and influx of magmatic fluids. Finally, we discuss the mechanisms of brucite marble emplacement and consider three possible ways of producing these rocks: (1) injection of dolomite with subsequent transformation to periclase marble and then to brucite marble; (2) injection of periclase marble with a following replacement of periclase by brucite or injection of brucite marble; (3) crustal water-rich carbonate melt. We favor models 2 and 3 and discuss their strengths and weaknesses.

Arguments in favor of magmatic or metasomatic genesis of the Katugin rare-metal ore deposit are discussed. The geological and mineralogical features of the deposit confirm its magmatic origin: (1) the shape of the ore-bearing massif and location of various types of granites (biotite, biotite–amphibole, amphibole, and amphibole–aegirine); (2) the geochemical properties of the massif rocks corresponding to A type granite (high alkali content (up to 12.3% Na2O + K2O), extremely high FeO/MgO ratio (f = 0.96–1.00), very high content of the most incoherent elements (Rb, Li, Y, Zr, Hf, Ta, Nb, Th, U, Zn, Ga, and REE) and F, and low concentrations of Ca, Mg, Al, P, Ba, and Sr); (3) Fe–F-rich rock-forming minerals; (4) no previously proposed metasomatic zoning and regular replacement of rock-forming minerals corresponding to infiltration fronts of metasomatism. The similar ages of the barren (2066 ± 6 Ma) and ore-bearing (2055 ± 7 Ma) granites along with the features of the ore mineralization speak in favor of the origin of the ore at the magmatic stage of the massif’s evolution. The nature of the ore occurrence and the relationships between the ore minerals support their crystallization from F-rich aluminosilicate melt and also under melt liquation into aluminosilicate and fluoride (and/or aluminofluoride) fractions.

Pyrochlore group minerals are the main raw phases in granitic rocks of the Katugin complex-ore deposit that stores Nb, Ta, Y, REE, U, Th, Zr, and cryolite. There are three main types: Primary magmatic, early postmagmatic (secondary-I), and late hydrothermal (secondary-II) pyrochlores. The primary magmatic phase is fluornatropyrochlore, which has high concentrations of Na2O (to 10.5 wt.%), F (to 5.4 wt.%), and REE2O3 (to 17.3 wt.%) but also low CaO (0.6&ndash, 4.3 wt.%), UO2 (to 2.6 wt.%), ThO2 (to 1.8 wt.%), and PbO (to 1.4 wt.%). Pyrochlore of this type is very rare in nature and is limited to a few occurrences: Rare-metal deposits of Nechalacho in syenite and nepheline syenite (Canada) and Mariupol in nepheline syenite (Ukraine). It may have crystallized synchronously with or slightly later than melanocratic minerals (aegirine, biotite, and arfvedsonite) at the late magmatic stage when Fe from the melt became bound, which hindered the crystallization of columbite. Secondary-I pyrochlore follows cracks or replaces primary pyrochlore in grain rims and is compositionally similar to the early phase, except for lower Na2O concentrations (2.8 wt.%), relatively low F (4 wt.%), and less complete A- and Y-sites occupancy. Secondary-II pyrochlore is a product of late hydrothermal alteration, which postdated the formation of the Katugin deposit. It differs in large ranges of elements and contains minor K, Ba, Pb, Fe, and significant Si concentrations but also low Na and F. Its composition mostly falls within the field of hydro- and keno-pyrochlore.

International audience; Our systematic investigation of the high sensitivity CW-Cavity Ring Down Spectra of 16O/18O ozone isotopologues at high vibrational excitation continues with the study of the 16O18O18O and 18O16O18O species. The first two papers of this series were devoted to the analysis of the same four bands of the 16O16O18O and 16O18O16O species in the 5930-6340 cm-1domain. Here, after a brief reminder of relevant experiment and theory, we report the analyses of two bands of 16O18O18O, vibrationally assigned as 2ν2+5ν3 and 2ν1+2ν2+3ν3_2 and three bands of 18O16O18O, assigned to 2ν1+2ν2+3ν3_1, 5ν1+ν3 and 3ν1+ν2+3ν3.They correspond to the highest vibration excitations observed so far for the 16O18O18O and 18O16O18O isotopologues. Altogether for the two new bands of 16O18O18O, 1214 rovibrational transitions were assigned up to Jmax=29 and for the three new bands of 18O16O18O, 948 rovibrational transitions were assigned up to Jmax=27. Observed line positions were fitted with root-mean squares deviations ranging from 0.005 to 0.011 cm-1, using effective Hamiltonian models accounting for dark state perturbations. The derived band centres and rotational constants are in good agreement with new theoretical calculations from the molecular potential function. The corresponding lists of 3365 lines are provided as Supplementary material.

Two types of carbonate and carbonate-silicate rocks: synmetamorphic marble melange and veined bodies in amphibolites, gabbroic rocks, and syenites are recognized in the Early Paleozoic Ol’khon collision system in the West Baikal region. The marble melange is characterized by the various size of the fragments of the mafic granulite, gneisses, metagabbros, and granites. It is suggested that the melange was injected into the silicate matrix as a result of a ductile flow. The calcite, dolomite, and carbonate-silicate rocks are characterized by their massive and fine-grained texture. They are often associated with coeval granite and dolerite dikes and occasionally reveal indications of carbonate-silicate mingling. It is suggested that carbonate and carbonate-silicate rocks were injected at late stages of the synmetamorphic tectogenesis. In isotopic composition, geochemistry, and mineralogy, these carbonate rocks differ from mantle carbonatites, and their origin is most likely related to the melting of carbonate rocks in the lower crust in the presence of aqueous fluid according to the model proposed by Lentz [29]. The shearing facilitated drainage of the lower crust and the upper mantle and made it possible to inject carbonate material to the upper level as a melt and a ductile mixture along with crustal granitic and mantle-derived basic melts. The injection carbonate rocks have been described from other metamorphic complexes, e.g., in the Caledonides of Norway and in the Himalayan collision system.

The infrared spectrum of 16O3 has been revisited in the ranges 3300–3600 cm−1 and 5200–5600 cm−1, recorded by the Fourier Transform Spectrometer of Reims, with an improved signal/noise ratio. In the lower spectral range the weak 2ν1+2ν2 band is observed and assigned for the first time. This allowed for completing the triad of strongly interacting (220), (121), and (022) states. The resonance interaction parameters for this triad were derived from the molecular potential energy surface using high-order Contact Transformation method. This involves Darling–Dennison resonances between (220) and (022) vibration A-states, and Coriolis resonances between (121) B-state and A-states. Altogether 18 coupling parameters were fixed to these theoretically predicted values that allowed avoiding problems of ambiguities while fitting strongly correlated parameters. The remaining small perturbations of a few Ka=5 transitions of the ν1+2ν2+ν3 band were explained by accidental Coriolis resonance of (121) with the (050) dark state. This mixed half theoretical/half empirical model (with 39 fitted and 77 theoretically constrained parameters) developed in this work for the first time allows an excellent description of 1897 line positions with the rms deviation ∼0.001 cm−1 closed to the experimental precision. The intensities of two new hot bands ν2+4ν3−ν3 and ν1+ν2+3ν3−ν1 that fall in this range were also observed and modelled, thanks to a better signal to noise ratio. In addition, the 5200–5600 cm−1 region has also been revisited, showing for the first time the (321) state which was considered as “dark” one in the previous analysis. Effective Hamiltonian parameters were derived for strongly coupled (213)/(114)/(321) upper states including (080) as a dark one. The transition moment parameters of all newly observed and assigned bands were derived resulting to average rms deviation for intensities of ∼8% and 13% for the cold and the hot bands, respectively, in the lower range and of ∼15% for the bands in the upper range that is close to experimental accuracy for weak transitions.

Carbonatites associated with syenites and subalkalic mafic rocks (lamprophyres) occur in the Himalayan continental collision zone, and this suggests their possible existence in other Phanerozoic collisional settings. The Early Paleozoic Ol’khon collisional system in Western Cisbaikalia is considered one of the possible occurrences. Subalkalic gabbroids as well as peculiar carbonate (brucite marbles) and calc-silicate rocks were found here, within the Tazheran massif of alkalic and nepheline syenites. Alkalic syenites, nepheline syenites, and calciphyres were dated at 471 Ma, 451–464 Ma, and 466 Ma, respectively, and their ages correspond to the main collisional events in the system. A geochemical description of igneous and carbonate rocks in the massif is provided. Close mapping showed unusual syenite and brucite marble combinations and the frequent vein or pipe-like form of carbonates and calciphyres corresponding to their magmatic intrusion. But carbonatite nature of the marble mentioned above does not fit their typical crustal geochemical features. Not ruling out the possibility of total change of geochemical signatures of mantle carbonatite in the collisional medium, we offer two other possible explanations for these facts: (1) melting of carbonate masses by syenite and mafic magmas, followed by carbonate melt intrusion into the upper crust, and (2) protrusion of carbonates into syenites and gabbroids at the late stages of the contact action of a silicate magma. In this case the above-mentioned carbonate structural features result from late recrystallization, whose mechanism is yet to be explained.

International audience; This paper is devoted to the third part of the analysis of the very weak absorption spectrum of the 18O 3 isotopologue of ozone recorded by CW-Cavity Ring Down Spectroscopy between 5930 and 6900 cm -1. In the two first parts [A. Campargue, A. Liu, S. Kassi, D. Romanini, M.-R. De Backer-Barilly, A. Barbe, E. Starikova, S.A. Tashkun, Vl.G. Tyuterev, J. Mol. Spectrosc. (2009), doi: 10.1016/j.jms.2009.02.012 and E. Starikova, M.-R. De Backer-Barilly, A. Barbe, Vl.G. Tyuterev, A. Campargue, A.W.Liu, S. Kassi, J. Mol. Spectrosc. (2009) doi: 10.1016/j.jms.2009.03.013], the effective operators approach was used to model the spectrum in the 6200-6400 and 5930-6080 cm -1 regions, respectively. The analysis of the whole investigated region is completed by the present investigation of the 6490-6900 cm -1 upper range. Three sets of interacting states have been treated separately. The first one falls in the 6490-6700 cm -1 region, where 1555 rovibrational transitions were assigned to three A-type bands: 3 ν2 + 5 ν3, 5 ν1 + ν2 + ν3 and 2 ν1 + 3 ν2 + 3 ν3 and one B-type band: ν1 + 3 ν2 + 4 ν3. The corresponding line positions were reproduced with an rms deviation of 18.4 × 10 -3 cm -1 by using an effective Hamiltonian (EH) model involving eight vibrational states coupled by resonance interactions. In the highest spectral region - 6700-6900 cm -1 - 389 and 183 transitions have been assigned to the ν1 + 2 ν2 + 5 ν3 and 4 ν1 + 3 ν2 + ν3 A-type bands, respectively. These very weak bands correspond to the most excited upper vibrational states observed so far in ozone. The line positions of the ν1 + 2 ν2 + 5 ν3 band were reproduced with an rms deviation of 7.3 × 10 -3 cm -1 by using an EH involving the {(054), (026), (125)} interacting states. The coupling of the (431) upper state with the (502) dark state was needed to account for the observed line positions of the 4 ν1 + 3 ν2 + ν3 band ( rms = 5.7 × 10 -3 cm -1). The dipole transition moment parameters were determined for the different observed bands. The obtained set of parameters and the experimentally determined energy levels were used to generate a complete line list provided as Supplementary Materials. The results of the analyses of the whole 5930-6900 cm -1 spectral region were gathered and used for a comparison of the band centres to their calculated values. The agreement achieved for both 18O 3 and 16O 3 (average difference on the order of 1 cm -1) indicates that the used potential energy surface provides accurate predictions up to a vibrational excitation approaching 80% of the dissociation energy. The comparison of the 18O 3 and 16O 3 band intensities is also discussed, opening a field of questions concerning the variation of the dipole moments and resonance intensity borrowing by isotopic substitution.

More than 5050 rovibrational transitions were assigned in the very sensitive CW-CRDS 18 O 3 spectra in the 5900–7000 cm −1 range leading to the first determination of 14 new vibrational band centres. Three bands correspond to the highest ozone states observed so far under high resolution. The good agreement between predicted and observed centres ( rms deviation of 1.1 cm −1 ) confirms the accuracy of the potential function previously determined from 16 O 3 data. At this energy range situated ∼20% below the dissociation energy, the small changes of masses associated with the 16 O 3 → 18 O 3 homogeneous isotopic substitution result in irregular isotopic shifts.

The far-infrared and middle-infrared emission spectra of deuterated water vapour were measured at temperatures 1370, 1520, and 1940 K in the ranges 320–860 and 1750–3400 cm−1. The measurements were performed in an alumina cell with an effective length of hot gas of about 50 cm. More than 3550 new measured lines for the D216O molecule corresponding to transitions from highly excited rotational levels of the (0 2 0), (1 0 0), and (0 0 1) vibrational states are reported. These new lines correspond to rotational states with higher values of the rotational quantum numbers compared to previously published determinations: Jmax = 29 and Ka(max) = 22 for the (0 2 0) state, Jmax = 29 and Ka(max) = 25 for the (1 0 0) state, and Jmax = 30 and Ka(max) = 23 for the (0 0 1) state. The extended set of 1987 experimental rotational energy levels for the (0 2 0), (1 0 0), and (0 0 1) vibration states including all previously available data has been determined. For the data reduction we used the generating function model. The root mean square (RMS) deviation between observed and calculated values is 0.004 cm−1 for 1952 rovibrational levels of all three vibration states. A comparison of the observed energy levels with the best available values from the literature and with the global predictions from molecular electronic potential energy surfaces of water isotopic species [H. Partridge, D.W. Schwenke, J. Chem. Phys. 106 (1997) 4618] is discussed. The latter confirms a good consistency of mass-dependent DBOC corrections in the PS potential function with new experimental rovibrational data.

International audience; The state of the art analyses of high-resolution ozone spectra and a critical discussion of line parameters updated since the previous review by Rinsland et al. [J Quant Spectrosc Radiat Transfer 2003;82:207–18] are presented. We focus on recent works revisiting improved measurements and analyses of Fourier transform spectra below 5600 cm−1 and review Cavity Ring-Down Spectroscopy measurements and analyses in the 5850– 7920 cm−1 spectral region which have been performed for 16O3 and all 18O enriched ozone isotopologues. Various issues related to resonance perturbations due to dark states are discussed as well as the issues concerning the accuracy of the experimental parameters, the data modelling and the data reduction. Comparisons of vibration levels determined from spectra analyses with predictions from the molecular potential functions are given. The procedures of empirical corrections for calculated line lists are described and the “intricate” question of absolute intensity determination is overviewed. Also, a review of deficiencies, challenge for improvements, and related works in progress are reported.

International audience; This work is part of a systematic investigation of the CW-Cavity Ring Down Spectra 16O/18O ozone isotopologues at high sensitivity (noise equivalent absorption αmin≈1×10-10 cm-1). A first contribution [Mondelain D, Campargue A, Kassi S, Barbe A, Starikova E, De Backer-Barilly MR, et al. J Quant Spectrosc Radiat Transfer, 2013;116:49-66] was devoted to the analysis of four bands of the 16O16O18O species of CS symmetry between 5930 and 6340 cm-1. Here we report the analysis of four bands of 16O18O16O of C2V symmetry, vibrationally assigned as 2ν1+2ν2+3ν3_1, 2ν2+5ν3, 5ν1+ν3 and 2ν1+2ν2+3ν3_2. They correspond to the highest vibration excitations observed so far for this isotopomer. Altogether, 1385 rovibrational transitions were assigned up to Jmax=31. Measured line positions were reproduced with rms deviations ranging from 0.005 to 0.013 cm-1, using effective Hamiltonian models accounting for dark state resonance perturbations. The derived band centres and rotational constants are found in good agreement with new theoretical calculations from the molecular potential function. The corresponding lists of 2124 lines are provided as Supplementary Material.

International audience; The first investigation of the very sensitive CW-Cavity Ring Down Spectra (noise equivalent absorption αmin≈1×10-10 cm-1) of 18O enriched ozone isotopologues is reported. The ozone generation from 18O enriched oxygen molecules resulted in six isotopic species. The contributions of the 16O16O18O/16O18O16O and of the 18O18O16O/18O16O18O isotopomers were separated using two partial pressures of 16O2/18O2 mixtures. In the 5930-6340 cm-1 range, the four dominant bands of 16O16O18O were vibrationally assigned as 2ν1+2ν2+3ν3_1, 2ν2+5ν3, 5ν1+ν3 and 2ν1+2ν2+3ν3_2. They correspond to the highest vibration excitations observed so far in an asymmetric CS ozone isotopologue. The rovibrational spectra for 18O enriched CS ozone species show specific features related to the nuclear spin statistics and to simultaneous symmetry allowed Coriolis and anharmonic accidental resonances, which are discussed. Altogether for the four new bands, 2155 rovibrational transitions were assigned up to Jmax=32. Observed line positions were fitted with rms deviations ranging from 0.005 to 0.01 cm-1 using effective Hamiltonian models accounting for dark state perturbations. The derived band centers and rotational constants are in good agreement with new theoretical calculations from the molecular potential function. The corresponding line lists are provided as Supplementary Material.

International audience; The absorption spectrum of the 18O3 isotopologue of ozone was recorded by CW-Cavity Ring Down Spectroscopy in the 6950-7125 cm-1 region. The typical noise equivalent absorption of the recordings is αmin ≈1×10-10 cm-1. The spectrum is dominated by three very weak bands: 3ν1+5ν3 near 7009 cm-1 and the ν2+7ν3 and 4ν2+5ν3 interacting bands near 7100 cm-1. In total 260, 206 and 133 transitions were assigned for the 3ν1+5ν3, ν2+7ν3 and 4ν2+5ν3 bands, respectively. The line positions of the 3ν1+5ν3 band were modelled using an effective Hamiltonian (EH) model involving two dark states - (6 0 1) and (2 5 2) - in interaction with the (3 0 5) bright state. The EH model developed for the ν2+7ν3 and 4ν2+5ν3 bands involves only the (0 1 7) and (0 4 5) interacting bright states. Line positions could be reproduced with rms deviations on the order of 0.01 cm-1 and the dipole transition moment parameters were determined for the three observed bands. The obtained set of parameters and the experimentally determined energy levels were used to generate a list of 984 transitions of the three bands which is provided as Supplementary Material.

The absorption spectrum of the 16 O 3 isotopologue of ozone was recorded in the 7000–7920 cm −1 region by using high sensitivity CW-Cavity Ring Down Spectroscopy ( α min ∼ 10 −10 cm −1 ). This report is devoted to the analysis of the 7300–7600 cm −1 region dominated by four A-type bands: 6 ν 1 + ν 3 centred around 7395 cm −1 , 3 ν 1 + 5 ν 2 + ν 3 and 2 ν 1 + 4 ν 2 + 3 ν 3 lying in the 7450 cm −1 region and 5 ν 1 + 2 ν 2 + ν 3 centred around 7579 cm −1 . 213 transitions of the 6 ν 1 + ν 3 band were assigned and the corresponding line positions were modeled using an effective Hamiltonian including a Coriolis resonance interaction between the (601) upper state and a A-type dark state. The two very close 3 ν 1 + 5 ν 2 + ν 3 and 2 ν 1 + 4 ν 2 + 3 ν 3 bands were analysed using a similar effective Hamiltonian scheme involving the anharmonic resonance coupling between the (351) and (243) states. For these two bands, 304 transitions were assigned. The modelling also includes a first Coriolis resonance interaction between the (351) bright state and the (530) dark state, and a second one between the (243) bright state and the (144) dark state. In the 7579 cm −1 region, 205 transitions of the 5 ν 1 + 2 ν 2 + ν 3 band were assigned and modelled taking into account the Coriolis resonance interactions between the (521) upper state and the (700), (342) and (280) dark states. The dipole transition moment parameters of the four analysed bands were determined by a least-squares fit to the measured line intensities. For the studied band systems, the effective Hamiltonian and transition moment operator parameters were used to generate line lists provided as Supplementary Materials .

International audience; The absorption spectrum of 18O 3 has been recorded in the 5930-6080 cm -1 region using CW-Cavity Ring Down Spectroscopy. 1888 transitions belonging to five bands have been assigned. Three of them are A-type bands: 2ν 2 + 5ν 3, ν 1 + ν 2 + 5ν 3 and 5ν 1 + ν 3, and two bands are of B-type: 2ν 1 + ν 2 + 4ν 3 and 4ν 1 + 3ν 2. Despite a complex spectral pattern perturbed by many rovibrational resonances, it has been possible to find a suitable effective Hamiltonian model reproducing all the transition wavenumbers (corresponding to 1016 energy levels) with an rms deviation of 9.5 × 10 -3 cm -1. A set of 721 line intensities was determined and fitted to derive the effective transition moment parameters. This set of parameters and the experimental energy levels were used to generate a complete line list of 2795 transitions allowing to generate synthetic spectrum in good agreement with the experimental spectrum.

The absorption spectrum of the 18 O 3 isotopologue of ozone has been recorded in the 6200–6400 cm −1 region by high sensitivity CW-Cavity Ring Down Spectroscopy. The spectrum is dominated by the 2ν 1 + 5ν 3 and 2ν 1 + 3ν 2 + 3ν 3 bands at 6270.6 and 6392.2 cm −1 , respectively which were treated independently. The rovibrational analysis of the 2ν 1 + 5ν 3 band has evidenced that the (2 0 5) upper state is perturbed by Coriolis resonance interactions with the (0 1 6), (3 0 4) and (3 5 0) states. A total of 659, 89, 131 and 5 transitions were assigned to the 2ν 1 + 5ν 3 , ν 2 + 6ν 3 , 3ν 1 + 4ν 3 and 3ν 1 + 5ν 2 bands, respectively. In the case of the 2ν 1 + 3ν 2 + 3ν 3 band, 344 transitions were assigned. Some of them were found perturbed by a Coriolis interaction of the (2 3 3) state with the (5 2 0) state. Overall, 681 energy levels were derived from the analysis of the 2ν 1 + 5ν 3 and 2ν 1 + 3ν 2 + 3ν 3 band systems. In both cases, a suitable effective Hamiltonian was elaborated, allowing accounting satisfactorily for the retrieved rovibrational energy levels. In addition, dipole transition moment parameters were determined by a least-squares fit to the measured line intensities. The effective Hamiltonian and transition moment operator parameters were used to generate a list of 1619 transitions given as Supplementary material .

The thick volume Stories [Povesti] by V. Rasputin, published by "Molodaia gvardiia" Publishers in 1976, could justly have been subtitled "selected," for it consists of four of his best works. The book is constructed unusually: the stories are arranged in an order opposite to that in which they had been written. Reading the book in order, one covers a path the reverse of that traversed over ten years by the writer himself, a path that delves almost to the very roots of his work: Farewell to Matera [Proshchanie s Materoi], 1976; Live and Remember [Zhivi i pomni], 1974; The Final Moment [Poslednii srok], 1971; and Money for Mariia [Den'gi dlia Marii], 1966.