Impact Identification of Carbon-Containing Carboniferous Clays on Surfaces of Friction Nodes

The article deals with issues related to the processes occurring in the wear result of steel surfaces of machine components in the presence of mineral grains. This type of destruction of cooperating surfaces usually takes place during the development of roadways or during mining of coal with use of longwall methods. Wear tests were carried out using the author’s ring-on-ring test stand, on which the conditions of real wear of machine components in the presence of rocks were simulated. An abrasive material based on clayey rocks with an admixture of carbonaceous substance was used in the tests. Based on the analyses, it was found that the obtained results related to the damages are typical for wear mechanisms: microcracking and low-cycle fatigue. On the surface of the steel samples, numerous effects of micro-cutting and chipping could be observed, which were the result of the clayey impact of wear products and grains of the mineral substance. Under friction, a part of the abrasive and the carbon substance were pressed into generated microcracks, which is directly related to their plastic properties. The remaining, unpressed part of the abrasive material was subjected to further friction effects caused by the pressure of the tester pocket load and the relative movement of both steel rings surfaces. After the friction tests, the mixture of silty carbon abrasive material was in the form of flat aggregates on the samples’ surfaces.

TYPES OF RIVERS FEEDING SEDIMENTARY BASINS ON THE SOUTHEASTERN EDGE OF THE SIBERIAN PLATFORM DURING THE RIPHEAN: SKETCH OF RECONSTRUCTION

Some geochemical features of fine-grained clastic/clay rocks of a number of Riphean formations of the Yudoma-Maya region of southeastern Yakutia are considered. A comparison of the distribution character of the data points of individual and average samples of clay rocks in the (La/Yb)N–Eu/Eu* and (La/Yb)N–Th diagrams, which show the composition of the bottom sediments of the estuarine parts of modern rivers of various categories, allowed us to make a number of conclusions. Thus, individual data points on the (La/Yb)N–Eu/Eu* diagram are concentrated mainly in the fields of bottom sediments of rivers feeding on erosion products of mainly sedimentary (categories 1 and 2) and volcanic rocks (category 4), as well as their overlapping zones. The average data point of the clay rocks of the Trekhgorka Formation in this diagram is located in the field of bottom sediments of rivers draining magmatic/metamorphic terranes (category 3). The average data points of shales of the Dim, Talyn, and Svetly formations are located in the zone of overlapping fields of bottom sediments of rivers of categories 1, 2, and 3, i.e., they contain erosion products of both sedimentary formations and magmatic and metamorphic complexes. This is quite well consistent with the real geological situation. At the same time, in the composition of clayey rocks of higher stratigraphic levels of Riphean, erosion products of magmatic/metamorphic terranes are either absent or their proportion is very small. On the (La/Yb)N–Th graph, most of the individual data points of Riphean clayey rocks tend to be in the fields 1, 2, and 4. Their average data points are mainly confined to the overlapping zone of the fields of bottom sediments of rivers of categories 1 and 2. The average data point of clay rocks of Ust-Kirba Formation is located in the field of bottom sediments of rivers that feed on products of erosion from rocks of volcanic provinces. It also does not contradict the real geological situation.

Bashkirian meganticlinorium: Late Riphean-Vendian hiatuses and possible transformations of basin provenances

The object of research. At the top of the Upper Riphean-Vendian sedimentary sequence of the Bashkirian meganticlinorium (western and central parts of the named structure, corresponding to the stratotypical locality of Riphean) there is a series of fairly well-established hiatuses – the pre-Uk and pre-Bakeevo. One can also assume the existence of the pre-Uruk and pre-Basa hiatuses. During each of them, the thin-grained aluminosiliciclastic’s distribution systems could be subjected to one or another transformations. However, whether this is actually the case is still not entirely clear. To solve this problem, the lithogeochemical features of clayey rocks of the Inzer, Minyar, Uk, Bakeevo and Basa formations are analyzed. If we assume that the hiatuses are accompanied by restructuring of the provenances, then this can/should lead to the appearance of more fresh, previously not subject to weathering, rock complexes at the paleo-watersheds. This circumstance should cause a change in the lithochemical characteristics of the thin-grained aluminosiliciclastics entering to the sedimentation area. Methods. The analysis of the lithogeochemical features of clayey rocks is based on data on the content of the main rock-forming oxides (about 40 analyzes) and rare and trace elements (total of 70 analyzes). These data make it impossible to investigate the change in different lithogeochemical parameters of clayey rocks (for example, CIA, GM, K2O/Al2O3, or others) from the bottom upwards through the section of each of the formations listed above, therefore we operate with the averages for the formation values of such parameters taking into account the values their standard deviations. Results and conclusions. On the majority of the discriminant diagrams used by us, the figurative data points of the Basa Fm. mudstones occupy a position that to some extent differs from the position of the clayey rocks of other formations. The only lithostratigraphic subdivision in the part of the Upper Precambrian sedimentary sequence of the Bashkirian meganticlinorium under consideration, whose clayey rocks demonstrate a chemically noticeably less mature, compared to the underlying formations, is the Uk Fm. It may be thought that this is the result of the appearance of more fresh (less transformed by weathering) rock complexes at the provenances. The scales of the pre-Bakeevo and pre-Basa breaks, if they existed, were, most likely, noticeably less significant.

C- and N-bearing Species in Reduced Fluids in the Simplified C–O–H–N System and in Natural Pelite at Upper Mantle P–T Conditions

C- and N-bearing species in reduced fluids weree studied experimentally in C–O–H–N and muscovite–C–O–H–N systems and in natural carbonate-bearing samples at mantle P–T parameters. The experiments reproduced three types of reactions leading to formation of hydrocarbons (HCs) at 3.8–7.8 GPa and 800–1400 C and at hydrogen fugacity (fH2) buffered by the Fe–FeO (IW) + H2O or Mo–MoO2 (MMO) + H2O equilibria: (i) Thermal destruction of organic matter during its subduction into the mantle (with an example of docosane), (ii) hydrogenation of graphite upon interaction with H2‑enriched fluids, and (iii) hydrogenation of carbonates and products of their reduction in metamorphic clayey rocks. The obtained quenched fluids analyzed after the runs by gas chromatography-mass spectrometry (GC–MS) and electronic ionization mass-spectrometry (HR–MS) contain CH4 and C2H6 as main carbon species. The concentrations of C2-C4 alkanes in the fluids increase as the pressure and temperature increase from 3.8 to 7.8 GPa and from 800 to 1400 C, respectively. The fluid equilibrated with the muscovite–garnet–omphacite–kyanite–rutile ± coesite assemblage consists of 50–80 rel.% H2O and 15–40 rel.% alkanes (C1 > C2 > C3 > C4). Main N-bearing species are ammonia (NH3) in the C–O–H–N and muscovite–C–O–H–N systems or methanimine (CH3N) in the fluid derived from the samples of natural pelitic rocks. Nitrogen comes either from air or melamine (C3H6N6) in model systems or from NH4+ in the runs with natural samples. The formula CH3N in the quenched fluid of the C–O–H–N system is confirmed by HR–MS. The impossibility of CH3N incorporation into K-bearing silicates because of a big CH3NH+ cation may limit the solubility of N in silicates at low fO2 and hence may substantially influence the mantle cycle of nitrogen. Thus, subduction of slabs containing carbonates, organic matter, and N-bearing minerals into strongly reduced mantle may induce the formation of fluids enriched in H2O, light alkanes, NH3, and CH3N. The presence of these species must be critical for the deep cycles of carbon, nitrogen, and hydrogen.

Synrift sandstones and clayey rocks: bulk chemical composition and location on a number of discriminant paleogeodynamic diagrams

The bulk chemical composition of synrift sandstones and associated clayey rocks has been analized, and the distribution of the fields they form has been studied on discriminant paleogeodynamic SiO2K2O/Na2O [Roser, Korsch, 1986] and DF1DF2 [Verma, Armstrong-Altrin, 2013] diagrams. The studied sandstones in terms of bulk chemical composition mainly correspond to greywacke, lititic, arkose and subarkose psammites; Sublitites and quartz arenites are also found. A significant part in the analyzed data massif consists of psammites, in which log(Na2O/K2O)-1.0; missing on the Pettijohn classification chart. This confirms our conclusion, based on the results of mineralogical and petrographic studies, that the sedimentary infill of rift structures unites immature sandstones, the detrital framework of which was formed due to erosion of local sources, represented by various magmatic and sedimentary formations. Synrift clayey rocks, compared with sandstones, are composed of more mature fine-grained siliciclastics. As follows from the distribution of figurative data points of clayey rocks on the F1F2 diagram [Roser, Korsch, 1988], its sources were mainly sedimentary deposits. The content of most of the main rock-forming oxides in the synrift sandstones is almost the same as in silt-sandstone rocks present in the Upper Precambrian-Phanerozoic sedimentary mega-complex of the East European Plate, but at the same time differs significantly from the Proterozoic and Phanerozoic cratonic sediments, as well as from the average composition upper continental crust. It is shown that the distribution of the fields of syntift sandstones and clayey rocks on the SiO2K2O/Na2O diagram does not have any distinct features, and their figurative data points are localized in the areas of terrigenous rocks of passive and active continental margins. On the DF1DF2 diagram, the fields of the studied psammites and clayey rocks are located in areas of riftogenous and collisional environments. We have proposed a different position of the border between these areas in the diagram, which will require further verification.