**2. Geotectonic position of the Greater Altai geological structures**

The Hercynian geostructure of the Greater Altai is located in the Central Asian mobile belt, in the northwest of the Altai-Alashan Modal Zone, and is bounded by deep faults in the northwestern direction (Loktevsko-Karairtyshsky and Chingiz-Saursky) which separate it from the Caledonides of the Gorny Altai (in the northeast) and Chingiz-Tarbagatai (in the southwest). The territory under consideration unites the geological structures of the Rudny Altai, Kalba-Narym, Western Kalba, Zharma-Saur and adjacent areas of Russia and China, the total length of which is more than 100 km with an average width of 3000 km in modern coordinates (**Figure 1**).

According to geotectonic zoning, they are separate blocks of the earth's crust or terranes that were welded together during the Hercynian collision and separated by a system of deep faults or structural zones (the Northeast, Irtysh, Zaisan, and so on). The latter are also considered as zones of upwelling and the entry of mantle material, and ore-bearing fluid flows into the earth's crust [2].

The deep structure of the region in terms of geological and geophysical data is sharply heterogeneous and is characterized by a multilayered earth crust (up to 50–55 km thick) with heterogeneous linear-mosaic blocks complicated by folded and discontinuous deformations.

The model of the GA deep structure is presented at the geological and geophysical section of the Altai geotraverse compiled by Lyubetskiy et al. (**Figure 2**) [2, 3]. The upper mantle (UM) is characterized by an inhomogeneous structure, and it lies at a depth of 38–55 km and has a dissected relief. Mohorovichich's (M) raising of the surface is also recorded in the northwestern flank of the suture zone (Gornostaevsk) and its southeastern continuation (Zaisan), and in the Rudny Altai (Rubtsovsk) [2].

structure development and processes of ore formation with the aim to develop new technolo-

The territory of East Kazakhstan is a unique geological area, in which many deposits of copper, lead, zinc, gold, silver, rare metals and rare earths, titanium, hydrocarbon raw materials and other minerals are concentrated. A powerful industrial infrastructure of mining and met-

The novelty of the study is further development of scientific idea of the Greater Altai (GA) geo-

microcontinents, horizontal displacement and coalescence of large tectonic blocks of the earth's crust (terranes) during the Irtysh-Zaisan paleobasin (a part of the Paleo-Asiatic ocean) degradation. A significant ore-controlling importance is attached to justification of belt placement of orebearing structures and deposits which were formed in various geodynamic settings and regimes. The tendency of ore deposit's belt distribution is manifested in the North American, Mexican, South China, Urals metallogenic provinces and other regions of Kazakhstan [4, 6]. Revealed ore belts within the territory of the Greater Altai regional ranks offer new opportunities for deposit forecasting and prospecting especially on poorly studied and closed territories.

**2. Geotectonic position of the Greater Altai geological structures**

The Hercynian geostructure of the Greater Altai is located in the Central Asian mobile belt, in the northwest of the Altai-Alashan Modal Zone, and is bounded by deep faults in the northwestern direction (Loktevsko-Karairtyshsky and Chingiz-Saursky) which separate it from the Caledonides of the Gorny Altai (in the northeast) and Chingiz-Tarbagatai (in the southwest). The territory under consideration unites the geological structures of the Rudny Altai, Kalba-Narym, Western Kalba, Zharma-Saur and adjacent areas of Russia and China, the total length of which is more than 100 km with an average width of 3000 km in modern coordinates (**Figure 1**). According to geotectonic zoning, they are separate blocks of the earth's crust or terranes that were welded together during the Hercynian collision and separated by a system of deep faults or structural zones (the Northeast, Irtysh, Zaisan, and so on). The latter are also considered as zones of upwelling and the entry of mantle material, and ore-bearing fluid flows into the

The deep structure of the region in terms of geological and geophysical data is sharply heterogeneous and is characterized by a multilayered earth crust (up to 50–55 km thick) with heterogeneous linear-mosaic blocks complicated by folded and discontinuous deformations. The model of the GA deep structure is presented at the geological and geophysical section of the Altai geotraverse compiled by Lyubetskiy et al. (**Figure 2**) [2, 3]. The upper mantle (UM) is characterized by an inhomogeneous structure, and it lies at a depth of 38–55 km and has a dissected relief. Mohorovichich's (M) raising of the surface is also recorded in the northwestern flank of the suture zone (Gornostaevsk) and its southeastern continuation (Zaisan), and in the


) of Kazakhstan and Siberian paleo-

gies of deep earth prognosis and prospect for ore deposits [1].

68 Tectonics - Problems of Regional Settings

structure formation during the Hercynian collision (C<sup>1</sup>

earth's crust [2].

Rudny Altai (Rubtsovsk) [2].

allurgical works and plants has been built in the region on their basis.

**Figure 1.** The Greater Altai geotectonic position in the structures of the Central Asian belt. 1—Ancient platforms and massifs; 2—Baikal; 3—Caledonian orogeny region; 4—Altai-Alashan area; and 5—position of the Greater Altai.

Deep mobile zones (DMZs) and associated systems of longitudinal-transverse faults which caused intensive transformations of the entire section of the EC and the upper mantle played a decisive role in magmatism origin and evolution, the spatial arrangement of volcanic and intrusive belts. The real differentiation of the upper mantle and the level of foci nucleation in the EC reformation column determined the composition and geochemical specialization of magmatism. The influence of the mantle plume evidently played a decisive role in the metallogenic specialization of Charskaya, West Kalbinsk and Zharma-Saur tectonic zones (Cr, Ni, Fe, Cu, Pb, Zn, Au, and so on).

These data are consistent with the views of a number of researchers on the relationship between plume magmatism and metallogeny in Tarim, Siberian, Emeishan, Central European and other large magmatic provinces (R.D. Dzhenchuraeva, 2015).

In fact, small deposits of magmatic Cu-Ni formation C2–3 (Maksut et al.) are known in the territory of East Kazakhstan, and the earlier action of the asthenolite plume was recorded in the Rudniy Altai (in the Devonian) and Chara zone during the stage of the Hercynian collision of C<sup>1</sup> -C<sup>3</sup> [3]. Later, in the lower Triassic, the Semeytauska volcano-tectonic construction of the trachybasalt-trachyriolite composition was formed under the influence of a local mantle plume. Therefore, the manifestation of mantle plumes in East Kazakhstan occurred, probably, repeatedly, and the mantle source of ore matter (Cr, Ni, Pt, Ir, Hg) is fixed in deposits of different types (copper-polymetallic, gold ore, rare metals and others). Consequently, it is also necessary to take into account the mantle plume models of the formation of ore-magmatic systems for metallogenic constructions in the territory of the Greater Altai.

The metabasalt layer (K surface) is fixed by amphibolites and hyperbasites fragments in the deep melange of Charskii, Irtysh-Markakol and other faults. In the axial part of the Rudny Altai, according to G.P. Nakhtigal's materials, the crust surface is elevated (at a depth of 22–24 km) bounded by Kalba-Narymsky (26–28 km) and Belousinsk-Sarymsaktin (28–30 km) edge deflections [2, 4, 5]. Metabasaltic layer elevations are also noted in the core zones of

**Figure 2.** Geological and geophysical section of the lithosphere at the Greater Altai according to Aleisk geotraverse. Granite-metamorphic layer: 1—Hercynides; 2—Caledonian; 3—Proterozoic. Intrusive bodies: 4—granites and granodiorites, plagiogranites; 5—diorite and gabbro; 6—metamorphic carbonaceous rocks. Meta basalt layer: 7 amphibolites; 8—granulites. The upper mantle: 9—primary; 10—ultrabasites; 11—eclogite garnet; 12—diamondiferous eclogite; 13—upwelling zones; 14—gravity field curves (Δg); (15) curves of the anomalous magnetic field (ΔT). Metallogenic zones: SSK, Syrektas-Sarsazan-Kobukskaya; ZhSK, Zharma-Saur-Kharatungskaya; ChZ, Charco-Zimunayskaya; WKK, West-Kalbinsk-Koksentauskaya; KNB, Kalba-Narym-Burchumskaya; IF, Irtysh-Fuyunskaya; RAA, Rudnoaltaisko-Ashalinskaya; GA, Gornyi Altai.

Zharma-Saursky and Chingiz-Tarbagatai belts. Evidently, this is a general pattern for the entire East Kazakhstan region.

with a suboceanic EK type of section (Charskaya, West Kalbinsk, the Irtysh zones). These tectonic zones, which have unequal tectonic magmatic activity, were saturated with basaltoid and

**Figure 3.** The layout of the faults of the Eastern Kazakhstan (by B.A. Dyachkov, G.P. Nakhtigal). 1—Deep longitudinal faults restricting tectonic structures and 2—their structure-formation zone; 3 and 4—regmatic system longitudelatitude prehercinian structural fault occurrence; 5—transverse deep faults of the Hercynian activation; 6—crushing zones; 7—ring structures; 8—thrusts; 9—fault-shifts; 10—direction of prevailing tectonic compression and 11—tension. Structural area (roman number in circles): I—Mountain Altai (Charyshskaya, Holzunsko-Chuiskaya), II—Beloubinsko-Sarymsaktinskaya (northeastern zone crumpling), III—Rudnoaltayskaya, IV—Irtyshskaya (Irtysh zone crumpling), (V) Kalba-Narymskaya, VI—Western Kalbinskaya, VII—Charskaya, VIII—Zharma-Saurskaya, IX—Sirektasskaya, X, XI—

Tectonics and Metallogeny of East Kazakhstan http://dx.doi.org/10.5772/intechopen.72745 71

Thus, the geodynamic model of the GA mobile belt development reflects a long and complex history of geological structure formation and emphasizes the intensity of ore-magmatic processes and metallogeny. As a result of polycyclic development of tectonic magmatic processes, the main epochs of ore formation have been outlined, reflecting vertical and lateral zonation within the ore belts and in general for East Kazakhstan. During the stepwise EC transformation and the migration of magmatic foci from the upper mantle, a homodromic evolution of the magmatic formations

granitoid matter in different ways with different geochemical specialization.

Chengis Tarbagataiskaya, XII—Pribalhashkaya.

The analysis of represented geological and geophysical data emphasizes the transverse heterogeneity of the deep structure of East Kazakhstan territory and different maturity of the EC in its different parts. Typical models of EC tectonic zone structure are reconstructed accordingly: (1) femic with increased capacity of metabasalt to 24–28 km (Chingiz-Tarbagatai, Rudnoaltayskaya and Zharma-Saurskaya zones); (2) sialic with a high thickness of metagranite layer up to 12 km and the EC up to 50–55 km (Kalba-Narymskaya, Syrektas-Sarzanskaya zone, Gorny Altai) and (3) interbedded femichesical—saliches on a heterogeneous (Precambrian-Caledonian) base

**Figure 3.** The layout of the faults of the Eastern Kazakhstan (by B.A. Dyachkov, G.P. Nakhtigal). 1—Deep longitudinal faults restricting tectonic structures and 2—their structure-formation zone; 3 and 4—regmatic system longitudelatitude prehercinian structural fault occurrence; 5—transverse deep faults of the Hercynian activation; 6—crushing zones; 7—ring structures; 8—thrusts; 9—fault-shifts; 10—direction of prevailing tectonic compression and 11—tension. Structural area (roman number in circles): I—Mountain Altai (Charyshskaya, Holzunsko-Chuiskaya), II—Beloubinsko-Sarymsaktinskaya (northeastern zone crumpling), III—Rudnoaltayskaya, IV—Irtyshskaya (Irtysh zone crumpling), (V) Kalba-Narymskaya, VI—Western Kalbinskaya, VII—Charskaya, VIII—Zharma-Saurskaya, IX—Sirektasskaya, X, XI— Chengis Tarbagataiskaya, XII—Pribalhashkaya.

with a suboceanic EK type of section (Charskaya, West Kalbinsk, the Irtysh zones). These tectonic zones, which have unequal tectonic magmatic activity, were saturated with basaltoid and granitoid matter in different ways with different geochemical specialization.

Zharma-Saursky and Chingiz-Tarbagatai belts. Evidently, this is a general pattern for the

**Figure 2.** Geological and geophysical section of the lithosphere at the Greater Altai according to Aleisk geotraverse. Granite-metamorphic layer: 1—Hercynides; 2—Caledonian; 3—Proterozoic. Intrusive bodies: 4—granites and granodiorites, plagiogranites; 5—diorite and gabbro; 6—metamorphic carbonaceous rocks. Meta basalt layer: 7 amphibolites; 8—granulites. The upper mantle: 9—primary; 10—ultrabasites; 11—eclogite garnet; 12—diamondiferous eclogite; 13—upwelling zones; 14—gravity field curves (Δg); (15) curves of the anomalous magnetic field (ΔT). Metallogenic zones: SSK, Syrektas-Sarsazan-Kobukskaya; ZhSK, Zharma-Saur-Kharatungskaya; ChZ, Charco-Zimunayskaya; WKK, West-Kalbinsk-Koksentauskaya; KNB, Kalba-Narym-Burchumskaya; IF, Irtysh-Fuyunskaya;

The analysis of represented geological and geophysical data emphasizes the transverse heterogeneity of the deep structure of East Kazakhstan territory and different maturity of the EC in its different parts. Typical models of EC tectonic zone structure are reconstructed accordingly: (1) femic with increased capacity of metabasalt to 24–28 km (Chingiz-Tarbagatai, Rudnoaltayskaya and Zharma-Saurskaya zones); (2) sialic with a high thickness of metagranite layer up to 12 km and the EC up to 50–55 km (Kalba-Narymskaya, Syrektas-Sarzanskaya zone, Gorny Altai) and (3) interbedded femichesical—saliches on a heterogeneous (Precambrian-Caledonian) base

entire East Kazakhstan region.

70 Tectonics - Problems of Regional Settings

RAA, Rudnoaltaisko-Ashalinskaya; GA, Gornyi Altai.

Thus, the geodynamic model of the GA mobile belt development reflects a long and complex history of geological structure formation and emphasizes the intensity of ore-magmatic processes and metallogeny. As a result of polycyclic development of tectonic magmatic processes, the main epochs of ore formation have been outlined, reflecting vertical and lateral zonation within the ore belts and in general for East Kazakhstan. During the stepwise EC transformation and the migration of magmatic foci from the upper mantle, a homodromic evolution of the magmatic formations and associated mineralization occurred. The change of sidero-chalcophile mineralization (Fe, Mn, Cu, Pb, Zn, Au, Ag) by chalcophile (Pb, Zn, Au, Ag, Bi, Sb, etc.) and lithophilic (Ta, Nb, Sn, W, Mo, TR, etc.) occurred from early to late epochs [6]. System analysis of the materials shows that in each metallogenic zone the maximum outburst of mineralization (with the formation of industrial deposits) occurred only in a certain geodynamic regime and in the age interval.

The post-collisional (orogenic) situation in the Permian was characterized by the activation of intra-plate tectonics and powerful development of granitoid magmatism, which is associated with deposits of rare metals and rare earths (Ta, Nb, Be, Li, Sn, W, Mo, TR, and so on). Deposits of rare metals are concentrated in the Kalba-Narym zone, Zharma-Saur, the Gorny Altai and other regions of Central Asia (China, Mongolia, the Urals, and so on) [13–15].

In the Cimmerian cycle, residual weathering crusts of nontronite profile (Ni, Co) accumulated in the Chara zone, kaolinite-hydromica (Au) in Western Kalba and Zharma-Saur, kaolinite (Ti, Zr) in northern Prizaisan (Karaotkel deposit) under continental rifting conditions. Deposits of coal and oil shale were formed in intermontane depressions (Karazhyra, Kenderlyk). Deposits of various minerals including placer gold, ilmenite, monazite, cassiterite and other minerals

As a result of study, it has been determined that geotectonic and metallogenic zoning is fully consistent and the following ore-bearing structures have been identified: a metallogenic province, ore belt, metallogenic zone (subzone), ore region, ore zone, ore site and ore field. The Hercynian geostructure of the Greater Altai which covers the territory of the Rudny Altai, Kalba-Narym, Western Kalba, Zharma-Saur and adjacent regions of Russia and China

Four ore belts have been determined within the Greater Altai by metallogenic zoning (**Figure 4**):

Chingiz-Tarbagatai belt in the southwest of the GA unites two metallogenic zones (West-Chingiz and East-Chingiz), and in the northeast there are Charyshskaya, Kholzun-Chuysko-

**The Rudny Altai belt** was formed on the destructured continental crust of the Gorny Altai during the Hercynian cycle, and the change of geodynamic regimes from the initial rifting

) was accompanied by a collision (C<sup>2</sup>

) and stabilization (Mesozoic-Cenozoic). The ore-control importance is given to a system of echeloned deep faults in the northwestern direction penetrating the activated upper mantle, which contributed to the entry of mantle-crustal magma and ore-bearing fluxes into the upper parts of the EC [3, 16]. Industrial copper-pyrite and pyrite-polymetallic deposits are concentrated in the core Rudny Altai zone of increased femininity of the EC section, the magmatic saturation and the density of mineralization and are clearly correlated with the elevation of the upper mantle, the metabasaltic layer, and the blocks of the Proterozoic and Caledonian


), orogenic activation (P<sup>1</sup>

Tectonics and Metallogeny of East Kazakhstan http://dx.doi.org/10.5772/intechopen.72745 73


**1.** Rudnoaltai copper-polymetallic (Fe, Mn, Cu, Pb, Zn, Au, Ag, and so on)

**4.** Zharma-Saursky multimetal (Cs, Ni, Co, Cu, Au, Hg, Mo, W, TR).

Sicikhe and Tsunghu-Chihuye zones adjacent to the Gorny Altai [8].

were formed in a Mesozoic-Cenozoic platform cover.

**2.** Kalba-Narym rare metal (Ta, Nb, Be, Li, Cs, Sn, W).


**3.** West Kalbinsky gold ore (Au, Ag, As, Sb).

**3.2. Metallogenic zoning**

(D1e) to the island-arc (D<sup>3</sup>

T1

basement.

is the largest.

The role of deep faults in the development of geological structures and metallogeny was considered in the works of many researchers (G.D. Azhgirey, A.V. Peive, N.P. Nekhoroshev, G.N. Shcherba, P.F. Ivankin, et al.). Deep faults had a long history of development, among which the Proterozoic, Caledonian and Hercynian fault systems as well as Cimmerian and Alpine (new and refurbished) are distinguished by age (location or intensive activation). The following systems also differ in direction: (1) longitudinally transverse (northwestern and northeastern), (2) longitude-latitudinal (regmatical), (3) diagonal, and (4) annular (according to space images interpretation) (**Figure 3**).
