The fragmentary fluidolites are represented by breccia, conglomerate-breccia and pseudo-conglomerates with the shape of fracture or irregular bodies, with a cross-cutting nature and flat, diagonal or steep subvertical bedding (Figure 2). The clastic material of the conglomerate-breccia is represented by limestone corresponding to the hosting stratum in terms of the composition; the fragments content varies from 30% - 40% to 70% - 80% and above. Their size varies within a wide range: from several centimeters to large boulders. The cement in the rocks of this zone is commonly aleuritic-sandy; the spots where red-color clayey material—argillizite serves as a cementing mass are present.

Abrupt difference in fragment sizes, their comminuted nature and lack of sorting are commonly observed in the cementing matrix.

The study of thin sections of psammite-psephite fluidolites testifies to the fact that they correspond to hosting organogenic limestones in terms of the composition. As we have found out, they, similar to hosting limestones, contain calcified remains of rock-forming calcareous algae of the Epiphyton sp. genus and the Proaulopora glabra Krasn species. The thin sections also show that the limestones have been penetrated by very thin calcite veinlets prior to fluidizate-explosive events (Figure 3).

The typical features of the fluidolites are typical for fluidolites localized in the carbonate stratum [8]: crosscutting shape of bodies; incomplete roundness of large fragments; non-roundness of fragments of the psammitic and aleuritic sizes (meanwhile, the bigger the fragment, the more rounded it is); nature of roundness (it can be observed both on gibbous and on concave spots); shape of

fragments (the fragments are represented by unflattened three-axis ellipsoids, which is common for typical boulders and pebble, but have the shape of a single-axis ellipsoid or even a ball); lack of sorting; abrupt increase in the size of fragments; comminuted exterior of small fragments (Figure 4); lack of sorting in the cementing matrix.

The rock of the matrix in this type of fluidolites has suffered imposed hematitization and partial crystallization. Hematite, the content of which in the samples varies from 0.49 wt% to 7.61 wt%, is distributed irregularly, in spots, and sometimes rhythmically around larger limestone fragments.

Before our studies, the nature of occurrence of aleurite-psammite-psephite rocks in the limestone stratum in the form of fractured or irregular bodies with a crosscutting nature, with flat, diagonal or steep subvertical bedding, was explained differently. They were considered olistostromes, neptunian clastic dykes or, as Yu.A. Zadisensky et al. [9] think, a carst lithified by breccia.

We think that in this case we deal with fluidolites [10]. Fluidolites, or fluid-explosive formations, commonly occur as the result of interaction of deep fluids with the rocks that are permeable for them. The occurrence of fluid flows is associated with abrupt pressure drop—the effect of decompression in fracture structures and their further compression intrusion as the result of activation of tectonic movements. This causes a specific type of transfer—solid-gaseous, solid-liquid-gaseous or solid-liquid [4] [8].

In our case, the autochthonous part of the Torgashino suite suffered the impact of low-temperature hydrotherms with high pressure. The magma centers that appeared during the Middle Paleozoic tectonomagmatic activation of the area, which started in the Middle Ordovician age and was associated with the occurrence of basaltoid and trachybasaltoid volcanism of the Imir volcanic complex

(O2-3 im), observed within the Kachinsko-Shumikhinskaya depression in the northwestern contour of the Eastern Sayan Mountains folding system, served as their source. At the same stage of tectonic development, a syenite intrusion of the Stolby complex was formed (State ..., 2000). The Later Ordovician age of the Stolby complex is defined both on the basis of breaking-through of co-magmatic effusives of the Imir suite and on the basis of available radioisotopic datings for the Stolby massif—U-Pb 449 ± 3 and 451 Ma, K-Ar 469 Ma [11].

One of the features of limestones in the formation under study is their secondary pleochroism. They are reddish-brown, brown, with color variation from light to dark of various intensity. Our studies showed that limestone is colored by ferruginized argillizite filling all permeable ways from very thin fractures to vein bodies (Figure 5). Limestone as such is crypto- and small-grained gray, with various tints, from common light-gray to rarer dark-gray. The rock structure is massive, spotty, sometimes brecciated and quite rarely indistinctly stratified.

The study of argillizites with the use of the X-ray phase analysis and synchronous thermal analysis allows identifying the features of the mineral composition of this fluidolite type (Table 1).

The data of the X-ray spectral elementary analysis of argillizites shows the following composition in % wt. (n/xmin-xmax/xav): O (18/52.30-58.76/56.01); Si (18/23.50-33.05/27.59); Al (18/5.63-11.47/8.83); Fe (18/0.83-4.85/2.59); С (17/1.44-3.32/2.52); К (18/0.04-1.64/0.75); Ti (18/0.11-0.76/0.44); Ca (18/0.03-1.64/0.45); Mg (18/0.01-0.56/0.21); Na (13/0.03-0.08/0.05); Mn (13/0.01-0.04/0.02); Р (1/0.03); Sr (1/0.02).

The cluster analysis of the obtained data showed the levels of correlations between the chemical elements. With the significance level of R05 = 0.49, valuable

Note – * – mineral remains after acidic dissolution.

negative correlations were established between oxygen and Fe, Ca, Mn, as well as silicon and Al, Fe, Ti, Ca. Positive valuable correlations were established between iron and Ca, Mn, and a very strong one between К and Mg.

Three positively connected groups of elements were identified: P-Sr-O-Si; K-Mg-C-Na; Fe-Mn-Ca-Ti-Al. They have negative relations with each other, and among them the relation of the latter group of elements with the first two ones is valuable (Figure 6). With exclusion of the impurity elements from consideration, the presence of valuable negative correlations between the mineral forming elements Fe–Ti and O-Si and between Si and Al can be stated.

Calcite crystals extracted from argillizites and veins of coarse-crystalline calcite mostly contain single-phase liquid inclusions, which testify to the hydrothermal nature of the mineral formation process. In some areas small double-phase inclusions can be found, containing a gas bubble and a phase of liquid water solution. The temperature of homogenization of double-phase inclusions (Figure 7) is 110˚С to 150˚С, which testifies to the low-temperature conditions

of formation of the rocks under study.

Carbonate metasomatosis occurring in the argillizite matrix filling cavities in limestone led to the formation of calcite onyxes. Rocks reflecting the initial stage of occurrence of carbonate onyx in argillizite vein bodies were found (Figure 8).

The study of thin sections of calcite onyxes collected from different veins shows a single mechanism of formation of banded aggregates. The growth of calcite aggregates in the argillizite mass starts from some surface (fracture wall, argillizite interlayer) with the formation of a zone of subparallel thin-columnar grains, and is completed as the result of geometric selection with the occurrence of larger cross-columnar crystals. Their growth is completed with the formation of idiomorphic heads which deform the argillizite substratum (Figure 9). When a part of the argillizite substratum is preserved in the form of an interlayer, the growth of the calcite aggregate reoccurs. As the result, we observe a rhythmic

aggregate with a distinct vector of its development.

In some cases brecciated onyx is found among the considered type of hydrothermalites. Clearly expressed disjunctive dislocations are its peculiar feature. Multiple fractures and crushed zones were cemented with later yellowish-white large-crystalline calcite or argillizite-altered calcite during further vein expansion (Figure 10). The color of onyx in such veins is commonly dark-brown or reddish-brown, which is associated with the presence of ferruginized argillizite. Therefore, brown bands have thin-banded, cryprocrystalline and even pelitomorphic structure, and the light (pink-white and white) ones have middle-banded structure.

The above-described studies show that clayey products in limestones are typical ferriferous argillizites of quartz-kaolinitic paragenesis. However, the mechanism of argillization is uncommon. Traditionally, argillization occurs by means of metasomatic rock replacement. In our case, limestones are not replaced but impregnated by clayey products.

Algillization of limestones is associated with the stage of tectonomagmatic activation of this region and with the occurrence of basaltoid and trachybasaltoid volcanism of the Imir volcanic complex (O2-3 im), which occurred within the Kachinsko-Shumikhinskaya depression in the northwestern contour of the Eastern Sayan Mountains folding system. Tectonic deformation and crushing of the carbonate stratum was accompanied by intrusion of pressurized low-temperature hydrotherms containing argillizite mass.

This process was of fluidizate-explosive nature and led to the occurrence of fluidolites [10]. In terms of the formation mechanism, argillizites can be considered as a specific type of fluidolites, which are formed as independent bodies and serve as cement of psammite-psephite calcareous fluidolites. In thin sections of the latter the clastic structure is typical not for carbonates only, but for quartz grains as well (Figure 11).

Geochronological tests of the absolute age with the 40Ar/39Ar method were conducted for solution of the problem of the fluidizate process age on the basis of the micaceous fraction of argillizites in the laboratory of isotope-analytical methods of the Institute of Geology and Mineralogy of the Siberian Branch of the Russian Academy of Sciences. The isotopic dating of argillizite fluidolites showed the correspondence of the time of their formation to the age of the Stolby syenite-granosyenite complex xO3st—458.1 ± 5.8 Ma.

Based on the performed studies fluidizate-explosive formations were identified for the first time within sedimentary carbonate strata. As was already mentioned above, tectonic activation of the Upper Ordovician age served as a release mechanism for the formation of fluidolites and associated hydrothermalites (calcite onyxes) in the stratum of the Torgashino formation. Intrusion of pressurized low-temperature hydrotherms with a high content of the argillizite mass occurred repeatedly after the phase of decompression of multiple fracture structures and crushed zones. This process was of fluidizate-explosive nature, reminding of mud volcanism in terms of the mechanism [12]. Its development led to the formation of various types of fluidolites. At the early stages coarse psephitic fluidolites were formed in the conditions of high pressure gradients and water and mud solution motion speeds (Figure 12).

Finer-fragmented carbonate material with hematitized cement and red clayey products calcitated to a different extent serve as a cementing matrix in them. The latter, as we found out, are hematitized quartz-kaolinite argillizites. Since argillizites do not have a metasomatic nature imposed on limestone but are impregnated products closely associated with clastic fluidolites, we referred them to the second type of fluidolites. Their formation took a long time—from early

pressurized and mobile mud flows to slowly moving viscous plastic masses containing carbonate fragments of various nature (sedimentary, hydrothermal). This is associated with compression pressure gradients in fracture structures, falling in time, and the duration of tectonic deformation processes.

The low temperature hydrothermal process which accompanied and completed the fluidizate-explosive process led to the occurrence of the third type of formations—hydrothermalites—calcite onyxes and coarse-crystalline calcite veins.