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Journal of geology, Geography And Geoecology
ISSN 2617-2909 (print) ISSN 2617-2119 (online)
Journ.Geol.Geograph.
Geology, 28(4), 673-691.
doi: 10.15421/111964
Leonid V. Isakov, Maria L. Isakova
Joum. Geol. Geograph. Geoecology, 28(4), 673-691.
Location pattern and genetic classification of granite pegmatites of the Ukrainian Shield
Leonid V. Isakov, Maria L. Isakova
National Technical University Dnipro Polytechnic, Dnipro, Ukraine, isakov_l@ukr.net
same names and including pegmatite fields of different mineralogical composition and geochemical specialization. The Volynski, Ingulski, Middle Prydniprovia, Western Pryazovia regions have rare-earth and rare-metal specialization presented by pegmatites of different origin and petrological and mineral composition and occurring in different structural and tectonic conditions, having different formation age, which allows a full classification scheme of the pegmatites of Ukrainian Shield to be given. These structures can be considered as having formed as a result of abyssal magmatic plumes. The geological-structural position of these megastructures with obvious signs of influence of certain abyssal processes on their formation supports this assumption. We present the main geological structural and genetic factors of formation of pegmatite-bearing megastructures of the Ukrainian crystalline core-area, these factors forming the basis of a classification scheme of pegmatites of Pre-Cambrian shields. We have systematized the pegmatites of the Ukrainian Shield , and designed their classification scheme . We have distinguished the following groups of pegmatites by the development of pegmatite-generating zones: - three genetic groups of pegmatites: ultrametamorphogenic, magmatogenic and metamorphogenic-meta-somatic; - six genetic subgroups of pegmatites: migmatic; autochthonous granite massifs; metamorphogenic and metasomatic displaced and formed pegmatites; multiphase intrusive granite massifs; multiphase intrusive alkaline massifs; multiphase granite batholiths. By the nature of pegmatite-bearing structures, the following structural groups have been singled out: granite-gneiss regional structures and domes; dome-synclinore and dome-trough plume-structures (subgroups: interdome synclinore and trough structures, in particular greenstone structures; intrusive domes and batholiths); specific tectonic zones of stress tensions.
Keywords: Ukrainian pegmatite province, Volyn, Ingulets, Middle Prydniprovia and Western Priazovia pegmatite regions, gneiss granite dome-shaped structure, synclinore, greenstone belt, pegmatites, classification of pegmatites.
Законом1рност1 розмпщення i генетична класифнкащя граштних пегматит1в Украшського щита
Л.В. 1саков, М.Л. 1сакова
Нацюнальний техн1чний утверситет «Днтровська полтехтка», Днтро, Украша, isakov_l@ukr.net
Анотащя. Розглянуто пегматити Украшського щита, 3aK0H0MipH0cri ïx формування та розмщення. Показано, щоУкрашський щит (УЩ) е пегматитовою провшщею, яка об'еднуе cîm райошв: Середньопридншровський, Захдаоприазовський, Схдаоприазовський, 1нгульський, Росинсько-Тжицький, Дшстерсько-Бузький i Волинський, яю вдаовдао охоплюють однойменш мегаструктури i несуть пегматжлж поля насичеш пегматитами рiзного мшералопчного складу i геоxiмiчноï спецiaлiзaцiï. Середньопридншровський, Захдаоприазовський, 1нгульський i Волинський райони представлен пегматитами рiзного генезису i петролого-мшералопчного складу та розмщуються в рiзниx структурно--тектошчних умовах, мають рiзний вж формування, що дае змогу на основi ïx систематизаци надати повноцшну класифжацшну схему пегматипв Украшського щита. Мегаструктури, що складають щ пегматшхж райони, можна вважати такими, що утворилися внaслiдок дiï глибинних магматичних плюмiв. На користь такого припущення свiдчить геолого-структурна позицiя мегаструктур з чггко вираженими ознаками впливу на ïx формування специфiчниx глибинних процеав. Вiдобрaженi основнi геолого-структурнi та генетичш чинники формування пегматитоносних грaнiтниx комплекав мегаструктур поклaденi в основу розробленоï клaсифiкaцiйноï схеми пегмaтитiв древнix докембршських щитiв. Проведено системaтизaцiю i складено клaсифiкaцiйну схему пегмaтитiв Украшського щита. За розвитком пегматитогенерувальних осередюв видшено: - три генетичнi групи пегматипв: ультрaметaморфогеннi, мaгмaтогеннi i метaморфогенно-метaсомaтичнi; - шють генетичних пiдгруп пегмaтитiв: мпматитовц автохтонних грaнiтниx мaсивiв; метаморфогенно i метасоматично зaмiщенi й утворенi пегматити; багатофазних
Received: 17.02.2019
Received in revisedform: 04.03.2019
Accepted: 20.09.2019
Abstract. The pegmatites of the Ukrainian Shield, their formation and occurrence are considered. It is shown that the Ukrainian Shield is a pegmatite province encompassing seven regions: Middle Prydniprovia, Western Pryazovia, Eastern Pryazovia, Ingulski, Rosynsko-Tikytski, Dnistersko-Buzki and Volyn, respectively encompassing megastructures of the
штрузивних граштних масив1в; багатофазних штрузивних лужних масив1в; багатофазних граштних батолтв. За характером пегматитовмюних структур видшено таю структурш групи: граштогнейсових регюнальних структур i купол1в; купольно-синклшорних i купольнотроговихплюмструктур (тдгрупи: м1жкупольшсинклшорш i трогов1, зокрема зеленокам'яш структури; штрузивш куполи i батолгги); специф1чних тектошчних зон стресових напруг.
Ключовi слова: Укратська пегматитова провтщя, Волинський, 1нгульський, Середньопридшпровський i 3axièmnpua3oecbKm пегматитовийрайон, гранiтогнейсовi куполи,синклторп, зеленокам'яш пояси, пегматити, систематизащяпегматитiв.
Introduction. Fundamental issues of geological and structural laws of formation of granite pegmatite fields and their occurrence in these fields lie at the basis of studies aimed at revealing the areas of development of pegmatite fields, their separate nodes and bodies and grounded prognostic exploration of rare metals and ceramic raw materials. Pegmatites of Pre-Cambrian complexes are the main indicators of commercially viable abundance of a range of rare metal elements, for some of them being the only indicator. In particular, according to statistics, from 73 to 92% of all reserves of Li, Rb, Cs, Be and Ta concentrated in pegmatites occur in Pre-Cambrian complexes.
There is a general classification of development process of pegmatite formation and Pre-Cambrian pegmatite field formation; this classification takes into account geological-structural and historical-geological features of earth crust development in the Archean, which allows further clarification of the sequence of geological processes influencing not only the structure and composition of separate pegmatite bodies and their conglomerates, but also the formation of pegmatite-bearing geoblocks of shields; this classification also allows one to answer certain fundamental general geological questions concerning the development of pegmatite-bearing territories and the earth's crust in general. Taking into account the link of pegmatites with both ultrametamorphic autochthonous granite complexes and intrusive granites, understanding of the laws of their formation will help clarify a set of important questions concerning the evolution of granitoid magmatism in the Pre-Cambrian. Analysis of recent papers. Since the first scientific description and study of pegmatites (by E.Patrin in 1791 and V. Severin in 1798) and the singling out of graphic granite as a separate mineral called "pegmatite" by R. Gauyi in 1801, several important stages of its study can be distinguished. The first important stage in pegmatite study started in the early 20th century and lasted till 1931, the year when "Pegmatites"
- a fundamental monograph by O. Fersman - was published. This period was characterized by the buildup of published research on the geology of pegmatites
- from the description of mineral forms and internal structure of bodies, to definition and characterization of pegmatite fields.
The next stage of pegmatite study, which started right after the above mentioned monograph and reached its climax in the mid 1940s, was connected with the expansion of commercial demand for rare metals, during which pegmatites, being the ores for these metals, were available and easily identified. The huge amount of scientific papers published in this period made it possible to create a separate branch of geological science - the study of pegmatites. At that time, on the basis of different viewpoints on the genesis of pegmatites there formed three scientific schools in the study of pegmatites. The representatives of the first school considered pegmatites to be the products of crystallization of residual molten-dilution of its intrusion from the main massif and gradual crystallization in the isolated system without significant introduction of external matter. V.Bregger, A.Lacrios, I.Gott and others were among the advocates of this theory, O.Fersman developed this idea, later supported by the research of K.Vlasov, I.Ginsburg, M.Solodov, I.Nedumov and others. Representatives of the second school regarded the formation of pegmatites as stemming from metamorphic and ultram-etamorphic transformations. These include P.Eskola, D.Korzhynski, N.Sudovikov, Yu.Sokolov and other researchers mainly studying Pre-Cambrian pegmatites. The third school interpreted pegmatites as the product of recrystallization and metasomatic transformation of aplites, bastard granite and formation of pegmatite bodies under the influence of postmagmat-ic solutions in the open system. The most well-known representatives of this school are V. Sheller, F. Hess, K. Lendon, O. Zavarytski, A. Nikitin and others.
Since the 1960s, a range of fundamental studies dedicated to the study of pegmatites has been published. The most important generalizing works that actually formulated the modern study of pegmatites are connected with names of I. Ginsburg, K.Vlasov, M. Solodov, I. Nedumov, M. Kuzmenko, A.Nikitin, V.Arhangelska, Yu. Sokolov, V. Petrov, A. Kalita, Ye. Lazarenko, V. Pavlyshyn, G. Rodionov, K. Babaiev, B. Shmakin, S. Shavlo, Yu.Yurk, L.Feldman and others. The appearance of fundamental works by the above researchers was the turning point indicating the beginning of the fourth generally theoretical period of development of the study of pegmatites. These works
formulated the main points of the pegmatite question, in particular: the geological structure of pegmatite belts, fields, nodes; the regularities of their occurrence and development; granite magmatism and pegmatite formation; influence of metamorphic, metasomatic, hydrothermal processes on the pegmatite formation; internal structure of pegmatite bodies and the conditions of their formation; mineral composition of pegmatites; geochemistry of pegmatites and evolution of geochemical processes; physical and chemical conditions of pegmatite formation; experimental modeling; practical issues of pegmatite exploration and use.
Historical study of pegmatites of the Ukrainian Shield dates back to the first quarter of the 20th century; however, serious research on them started only 70 years ago. During 1930-50s the research works were scattered and mainly aimed at the study of pegmatites as ceramic raw materials, except for the Koro-stensky pluton, where starting from 1931 geological-prospecting operations of chamber pegmatites began. Systematic research on pegmatites as rare metal raw materials started in the 1960s. Thanks to the joint efforts of industrial and research groups, in 1960-90s and at the beginning of the 21st century, large- and medium-scale geological and prognostic-metallogen-ic maps of the Eastern part of the Ukrainian Shield were created, a huge amount of factual material about different types of pegmatites was collected, the main directions of prospecting works for rare-earth metals, quartz and jewelry raw materials (topaz, beryl), and ceramic raw materials in pegmatites were determined. The following outstanding researchers of pegmatites should be mentioned: L.Lavrynenko, V.Kychurchak, L.Isakov, O.Koval, G.Lepigov, N.Viatkin, P.Shramko, S.Shutov, V.Kyshurchak, V.Pustovoitov, V.Kinshakov, V.Shpilchak, B.Ivanov, O.Lysenko, V.Lysenko, O.Makivchuk,V.Bezvynni, G.Lepigov, V.Mokiets.
At the same time, pegmatites of the Ukrainian Shield were studied by the following scientists and researchers; E.Lazarenko, M.Semenenko, Yu.Yurk, V.Pavlyshyn, B.Zatsiha, L.Isakov, M.Ivantyshyn, G.Kniazev, V.Kichurchak, L.Lavrynenko, K.Lytov-chenko, K.Rozanov, S.Shavlo, N.Yashchenko and others. Their findings are presented in numerous papers and monographs, in particular: E.Lazarekno, V.Pavlyshyn, Yu. Sorokin."Mineralogia i genesis ka-mernyh pegmatitov ["Mineralogy and genesis of chamber pegmatites"], 1973; Ye.Lytovchenko."Granitnie pegmatity Zapadnogo Priazovia" ["Granite pegmatites of Western Pryazovia"], 1976; K.Rozanov, L.Lavrynenko."Redkometalnie pegmatity Ukrainy" ["Rare metal pegmatites of Ukraine"], 1979; S.Shavlo, G.Kniaev, S.Kirikilitsa."Granitnye peg-
matity Ukrainy" ["Granite pegmatites of Ukraine"], 1984; "Kriterii prognozirovania mestorozhdeni Ukrainskogo shchita i ego obramlenia" ["Criteria of forecasting deposits of the Ukrainian Shield and its margins"], 1980 (ed. by M.Semenenko); "Mineralogia Priazovia" ["Mineralogy of Pryazovia"], 1980 (ed. by Ye.Lazarenko); L.Isakov "Polia granitnyh pegmatytiv Zakhidnogo Pryazovia" ["Granite pegmatite fields of the Western Pryazovia"], 2007 and oth. Under the supervision of S.Shavlo, Institute of Mineral Resources, maps of the pegmatite fields of the Ukrainian Shield were created and criteria of forecasting pegmatite related mineralization were developed (1973, 1980); in 2004 this work was resumed under the supervision of L. Isakov in Ukrainian State Geological Prospecting Institute, resulting in 2008 in a topical report on pegmatites of the Western Pryazovia and Middle Pryd-niprovia. Unfortunately, further work was suspended due to the lack of financing.
Geological-prospecting and scientific research work resulted in the discovery of a group of Volyn deposits of chamber pegmatites (quartz, topaz, beryl) within the Korostensky pluton of the Volyn megablock (in the 1930s - 1940s); in the 1960s came the discovery of the rare metal deposit of pegmatites "Krutaia Balka" attributed to the central part of So-rokynska tectonic zone; in the 1980s - 1990s, the Shevchenkivske deposit of lithium pegmatites within the Shevchenkivsko-Fedorivska structure was discovered; discoveries included a range of prospective occurrence of rare metals in pegmatites of the Sorokyn-ska structure, the Shevchenkivska and Fedorivska structure and rare earth metals in pegmatites of the Gaichur structure of the Western Pryazovia mega-structure; occurrences of rare-metal pegmatites of the Komendantivska and Zhovtovodska structure of the Middle Prydniprovia megablock; rare metal pegmatites of the Ingulski megablock: Polokhivske and Stankuvatske pegmatite fields (Polohivske, Nadia and Stankuvatske deposits);occurrences of rare-metal pegmatites of Mostove and Vys pegmatite fields. General information and regionalization of Ukrainian pegmatite province. The generally accepted hierarchy scheme of pegmatites is as follows: pegmatite > pegmatite node > pegmatite field > pegmatite belt > pegmatite region> (pegmatite area)>pegmatite province. According to this scheme, the Ukrainian Shield is a pegmatite province encompassing seven regions: Middle Prydniprovia, Western Pryazovia, Eastern Pryazovia, Ingulski, Rosynsko-Tikytski, Dnistersko-Buzki and Volyn (Fig. 1, geological basis (Tectonic map, 2006, Drannyk, 2003), respectively encompassing megastructures of the same names.
Fig. 1 The map of regionalization of Ukrainian pegmatite province [28]
We combine the Western Pryazovia and Middle Prydniprovia regions (Isakov, 2013) into the Eastern Ukrainian pegmatite area, as both these structures had a similar or probably common development during its mass formation of pegmatites, which resulted in the formation of pegmatite belts (Fig.2).
We also, for our purpose, have combined the Ro-synsko-Tikytski and Dnistersko-Buzki regions into the Western Ukrainian pegmatite area. These regions at the moment are associated with ceramic specialization with rare earth geochemical specialization .However, on the basis of separate geological-structural constructions of the Rosynsko-Tikytski mega-structure (greenstone formations are not excluded), and taking into account the considerable influence of granite massifs of the Korostenski pluton in its northwestern part, the development of pegmatite fields of rare metal specialization is quite possible within the
structure. Nevertheless, the pegmatites discovered within the boundaries of this area are homogeneous and are attributed to ultrametamorphic migmatite and granite complexes. We are not going to focus on these two areas except for the above statement. Taking into account the geological-structural development of the Eastern Pryazovia area, and the presence of complex granite and alkaline intrusions within its boundaries, this area also belongs to the promising areas containing rare-earth pegmatites, although, unfortunately, considerable occurrences have not been found so far.
The Volynski, Ingulski, Middle Prydnipro-via, Western Pryazovia regions have rare-earth and rare-metal specialization. These structures can be considered as having formed as a result of abyssal magmatic plumes. The geological-structural position of these megastructures with obvious signs of influence of abyssal processes on their formation is
Fig. 2. Contour map of geological structure of the Eastern part of the Ukrainian Shield.
1 - two-feldspar granites of the Demurski, Tokivski, Mokromoskovski, Dobropilski, Saltychanski and Yanvarski complexes; 2 - plagi-ogranites, tonalites of Surski, Saksaganski and Shevchenkivski complexes; 3 - metamorphic series (Aulska and Western Pryazovska) and ultrametamorphic complexes (Slavgorodski, Novopavlivski and Dnipropetrovski) of dome structures; 4 - metamorphic formations (Vovchanska and Dragunska), Central Pryazovia series and ultrametamorphic complexes (Remivski and Tokmatski) of sutural zones; 5 - metamorphized igneous-terrigenous complexes of trough structures of greenstone type (Konkska, Bilozerska, Osypen-kivska series and Novogurivska, Ternuvatska, Kosivtsivska formations); 6 - terrigenous complexes of fault-line superimposed structure (Kryvorizka series, Guliapilska suite); 7 - gabbro, monzonites, syenites of Southern Kalchytski and Oktiabrski alkaline intrusive complexes; 8 - local abyssal fracture; 9 - other fractures; 10 - geological boundaries; 11 - notional boundaries of greenstone belts.
in favour of this assumption. The formation process of these megastructures from the point of view of abyssal magmatic plumes is considered in our previous publications (Isakov, 2017). It should only be noted that the structural-geological body of the above mentioned megastructures is determined by granite-gneiss domes with the development (in some structures) in their central parts with large granitoid batho-lites of complex internal structure and wide range of material composition, surrounded by synclinal- and graben-like trough structures composed of igneous-sedimentary formations metamorphosed in the conditions of greenschist and amphibolite facies of regional metamorphism. The analysis of reconstruction of the sequence of geological processes resulting in the formation of these interrelated structures allows us to assume there was a series of stages in the formation of pegmatite fields, which can be divided into two main periods. The first period was associated with ultrametamorphic processes and led to the formation of ceramic pegmatites in ancient granite-gneiss dome structures with the formation of large areas, mostly of
isometric fields; while the second period of pegmatite formation is clearly associated with the process of forming granite intrusions and batholiths- pegmatites of this period are mostly associated with narrow trough structures developed around granite batholiths and granite-gneiss domes, and they could be formed in several stages.
The main factors influencing the formation and composition of pegmatites of the Ukrainian Shield.
Based on the above considerations, we look at characteristics of four pegmatite regions (Volynska, In-gulska, Middle Prydniprovia and Western Pryazovia megastructures) presented by pegmatites of different origin and petrological and mineral composition and occurring in different structural and tectonic conditions, having different ages of formation, which allows us to make a full classification scheme of the pegmatites of the Ukrainian Shield.
Western Pryazovia megastructure. The gradual interrelated development of the megastructure (Isa-kov, 2011, Isakov, 2012) respectively affected the formation of its tectonic structures of a higher order,
I - two-feldspar granites of Dobropilski, Saltychanski and Yanvarski complexes; 2 - plagiogranites, tonalites of Shevchenkivski complex; 3 - metamorphic Western Pryazovia series and ultrametamorphic Novopavlivski complex of dome structures; 4 - metamorphic formations (Vovchanska and Dragunska), Central Pryazovia series and ultrametamorphic complexes (Remivski and Tokmatski) of sutural zones; 5 - metamorphized igneous-terrigenous complexes (Osypenkivska series and Novogurivska, Ternuvatska, Kosivtsivska formations) of trough structures of greenstone type; 6 - terrigenous complexes of fault-line superimposed structure (Guliapilska suite); 7 - local abyssal fractures; 8 - other fractures; 9 - geological boundaries; 10-14 - notional boundaries: 10 - of pegmatite belts; 11 - of ceramic pegmatite fields; 12 - of rare metal pegmatite fields; 13 - of rare earth pegmatite fields; 14 - of pegmatite fields of unspecified specialization (presumably rare metal, rare earth specialization); 15 - pegmatite belts:
II - Shevchenkivsko-Vislynski; III - Sorokynsko-Gai-churski; 16 - ceramic pegmatite fields: 16 - Kamensko-Vovchanske; 18 - Guliaipilske; 25 - Temriuk-Korsak-ske; 27 - Yeliseivske; 8 - Tokmachanske; 17 - rare metal pegmatite fields: 17 - Shevchenkivske-Fedorivske, 26
- Sorokynske; 18 - rare earth pegmatite fields; 19 - Gai-churske, 21 - Kuibyshevske, 23 - Vislynske; 19 - specified pegmatite fields and fields of unspecified rare metal, rare earth specialization: 17a - Vovchanske, 20 - Pav-lilvske, 22 - Chystopilske, 24 - Dragunske, 29 - Molo-chanske; 20 - deposits and ore occurrences of rare earth associated with pegmatites: 5 - Gaichurska group, 6 -Kuibyshevske, 7 - Mogyla Visla; 21 - deposits and ore occurrences of rare metals associated with pegmatites: 1
- Voskresentki, 2 - Voskresentki-2, 3 - Shevchenkivske, 4 - Mokroialynski, 9 - Kruta Balka, 10 - Golubi Skeli; 22 - deposits and ore occurrences of ceramic raw materials associated with pegmatites: 8 - deposit group (Balka Velykogo Taboru, Dalnia Kamchatka, Balka Glyboka, Dolynske, Yelisiivske and others.)
Fig. 3 Geological map of Western Pryazovia pegmatite region.
the granitoid formations and the pegmatites associated with them. Due to the influence of the deep processes caused by the action of the magmatic plume, the Ovchanskiy and Saltychansky middle granitoid-gneiss domes were formed; and as compensatory structures around them, the Oryhivsky-Pavlogradsky and Maloenysolsky synclinores are represented by a narrow isocline folded structure (Fig. 2). Granite-gneiss domes are composed by the formations of the Western Priazovian series of the early Archaean and heterogeneous granite rock masses - Saltychan-sky and Gulyaypilsky represented by plagiogran-ites, tonalites, diorites, occasionally gabbro of the Shevchenkivsky and Obotoknovsky complexes of the late Archean age (2.8 billion years). The syncline structures, united into a single zone in the central part, are composed of the Vovchanska, Dragunska, and
Novopavlivska formations of crystalline schist and gneisses of different composition of the amphibolite stage of metamorphism, and the Central Pryazovian series of high-alumina formations, whose age varies from the early Archaean to the Early Proterozo-ic, which may explain the complex structure of the synclinores. Greenstone structures are located in the junction zones of synclinores and dome structures and form two sub-parallel segmental semicircular greenstone belts - the Shevchenkivsko-Berestovsky and the Sorokinsky-Gaichursky. The former consists of the following trough structures: Shevchenkivska, Fe-dorivska, Vovchanska and Dibrovska surrounded by the Vovchansky dome; and the Pavlivska and Bere-stovska structures within the Maloyansilsky synclino-ria. The Sorokinsko-Gaichursky greenstone belt is composed of the Sorokinska and Dragunska trough
Fig. 4 Geological map of Shevchenkivski node of rare metal pegmatites:
1-4 - pegmatites: 1 - albite-spodumene, albite-petalite-spodumene; 2 - albite; 3 - albite-microcline; 4 - microcline and microcline-oligoclase; 5 - muscovite-biotite, amphibole-muscovite-biotite fine- and medium-grained, muscovite-biotite pegmatoid granites; 6-17 - Ternuvatska rock mass, crystal slates: 6 - biotite, 7 - amphibol-biotite, 8 - muscovite-biotite, 9 - sillimanite-muscovite-biotite, 10 - garnet-biotite, 11 - garnet- sillimanite-biotite, 12 - garnet-muscovite-biotite, 13 - sillimanite-garnet-muscovite-biotite, 14 - biotite tourmalin bearing, 15 - quartz-sericitic; 16 - epidote- and quartz bearing scarified calciphyre; 17 - quartz-garnet-epidote-pyroxene calc-silicate hornfels; 18 - boundaries between subsections of different age: a - determined, 6 - anticipated; 19 - boundaries between lithological types of rocks; 20 - fractures: a - determined, 6 - anticipated; 21 - numbers of pegmatite bodies.
structures surrounded by the Saltychansky granite dome and Kuibyshevska, Gaichurska, Kosivtsivska ones-surrounded by the Guliaipilsky granite dome. They are close to the composition of volcanogenic-terrigenous rocks of the Osipenkivska series and the Kosivtsivska and Ternuovatsky formations of the Meso-Neoarchean era, metamorphized in conditions from the greenstone to the amphibolite facies of the regional metamorphism. Along these structures are developed granite masses of the Yanvarsky and Saltychansky complexes, whose age according to various estimates is 2.6-2.2 billion years. The structures that form these green-stone belts are the main reservoir for rare-metal and rare-earth pegmatites (Fig. 3).
Concerning the pegmatite formation stages within the Western Pryazovia megastructure, the first stage of pegmatite formation is ultrametamorphism that developed intensely in the final stage of forma- tion of the dome-synclinore structure of Western Pryazovia (Remivski ultrametamorphism). In this period pegmatites were formed as neosoms in the process of partial melting of rock complex of both the ceramic pegmatite field around it and within autochtonous granite massifs.
Pegmatite formation of the second stage is associated with the establishing of granite-gneiss domes and bedding of Shevchenkivski plagiogranite massifs. The establishment of allochtonous plagiogranite massifs of this complex was accompanied by bedding of the bulk of ceramic pegmatites with wide fields of formation (Yeliseivske, Temriuk-Korsakske, Vovchan-
ske and Guliaipilske) located both in granite massifs and in rock complexes of the Western Pryazovian, and sometimes in Vovchanska and Dragunska rock masses.
The establishment of multi-stage intrusives of two-feldspar granites of Yanvarski, Dobropilski and Saltychanski complexes (the third stage) was accompanied by intrusion and penetration of a significant mass of pegmatite matter in the weakened zones of trough structures of greenstone belts with the formation of pegmatites of different types (in particular, rare metal and rare earth) depending on the time, depth of their intrusion and specialization of the massifs. Resulting from these processes there formed the fields of rare metal and rare earth pegmatites: Shevchenkivske, Fedorivske, Vovchanske, Sorokynske, Gaichurske and others, in their turn forming the Sorokynsko-Gaichurski and Shevshenkivsko-Berestivski pegmatite belts. They are associated with such well-known deposits of rare metal pegmatites as Shevchenkivske (Isakov, 2013) (Fig. 4) and Kruta Balka (Rozanov, 1979) (Fig. 5).
Middle Prydniprovia megastructure is attributed to the category of specific lower Pre-Cambrian geo-structural elements of the Earth crust - granite-greenstone areas or folded-dome greenstone belts (Bobrov, 2002, Sivoronov, 1983, Shcherbakov, 2005) associated with large pegmatite provinces in other shields -Yilgarn in Australia, Winnipeg-Nipigon Abitibi in North America and others. The megablock is characterized by relative time sequence of change of geo-
Fig. 5 Schematic geological map of Kruta Balka pegmatite node [14]:
1 -quartz veins; 2 - pegmatite bodies; 3 - metaultrabasite; 4 - slightly metamorphized biotite, amphibolic and other types of slates; 5 - quartzites; 6 - metagravelite and metaconglomerate; 7 - diorite-granodiorite; 8 -fractures; 9 -geological contours.
logical conditions similar to the above provinces in the formation of rock complexes as well as their effect on the development and establishment of pegmatite fields.
The megastructure includes the following closely interconnected structural units (Fig. 6): 1) Saksagan-sky, Zaporizky, Pyatihatsky, Demurinsky, Slavgoro-dsky and other granite-gneiss and migmatite-gneiss domes made of supracrustal formations of the Aulska series and Dnipropetrovsk and Slavgorod plagiogran-ite-migmatite and endebit-charnokytoid complexes; 2) the Krivorizko-Kremenchutsky, Bazavlutsky and Konksko-Belozersky green-stone belts are composed
1[0
I ^ b
Fig. 6 Schematic geological-structural map of Middle Prydniprovia pegmatite region
1 - two-feldspar granites of Demurski, Tokivski, Mokromoskovski complexes; 2 - plagiogranites, tonalites of Surski and Saksaganski complexes; 3 - metamorphic series (Aulska) and ultrametamorphic complexes (Slavgorodski and Dnipropetrovski) of dome structures; 4 - metamorphized igneous-terrigenous complexes of trough structures of greenstone type (Konkska and Bilozerska series); 5 - terrigenous complexes of fault-line superimposed structures (Kryvorizka series); 6 - abyssal regional fractures; 7 - fractures; 8 - geological boundaries; 9 - notional boundaries of pegmatite belts that encompass: a - established pegmatite fields; 6 - conditionally established and anticipated pegmatite fields; 10-14 - notional boundaries of pegmatite fields: 10 - ceramic, 11 - rare metal, 12 - unspecified (presumably of rare metal and rare earth) specialization; 13 - pegmatite belts: I - Komendantivsko-Zhovtovodsko-Mokromoskovski; 14 - ceramic pegmatite fields: 2 - Piatyhatske, 4 - Krynychanske, 8 -Bazavlutske, 11 - Tokmatske; 15 - rare metal pegmatite fields: 1 - Komendantivske, 3 - Mykolaivke, 5 - Zhovtovodske, 6 -Gannivske; 16 - pegmatite fields of specified and unspecified (presumably) of rare metal, rare earth specialization: 7 - Ternivske, 10 - Vysokopilske; 17 - mineral occurrence of rare metals associated with pegmatites.
by the Vysokopilsky, Chortomlitsky, Sofievsky, Verk-hovtsy, Sursky, Zhovtovodsky and other green-stone downfolds composed of apo-volcanogenic formations of the Konkska series and apo-sedimentary formations of the Bilozerska series; 3) plagiogranite rock masses of the Saksagansky and Sursky complexes connected with green-stone structures; 4) multi-phase granite massifs: Demurinsky, Mokromoskovsky, Tokivsky, Orilsky and others related to green-stone structures. By structural form and history of its formation, the Middle Pridniprovian megastructure is the plume structure of the Ukrainian Shield (Isakov, 2017).
The lower age limit of the Konkska series is de-
termined by the age of zirconium from the metavol-canites of the Surska suite- 3177 Ma upper age limit - by the age of zirconium from plagiogranites of the Sursky complex - up to 2960 Ma. The lower age limit of the Bilozerska series is determined by zirconium from meta-keratophyres - 3000 Ma. The upper age limit of the entire green-stone rock mass is determined by the age of the youngest granite of the Demurinsky
and the Mokromoskovsky complexes that transect it - 2850-2700 Ma (Shcherbak, 2005).
The fields of ceramic pegmatites located immediately within granite-gneiss domes indicate the first stage of formation of pegmatites in the period of ultra-metamorphism of dome structures of rock complexes. In outcrops there is discovered close or immediate location of these pegmatites in migmatites and granit-
Fig. 7 Geological map of the Komendantivska greenstone structure and location of the same-name pegmatite field, node and ore occurrence within in:
1 - formation of the Kryvorizka series; 2 - diabase dikes; 3 - granites of the Tokivski complex; 4 - plagiogranites of the Surski complex; 5-gabbro-diabase6-8 - formation of Surska suite: 6 - amphibolites; 7 - amphibole, amphibole-biotite crystal slates; 8 - talk-tremolite-serpentine slates; 9 - plagiomigmatites of the Dnipropetrovsk complex; 10 - formation of the Bazavlutska rock mass; 11 -geological boundaries; 12 - fractures; 13 - Komendantivski node of rare metal pegmatites; 14a - Komendantivske field of rare metal pegmatites; 146 - anticipated field of rare metal pegmatites; 15 - pegmatite veins; 16 - Komendantivski ore occurrence of tantalum and lithium.
9CZZ] '°CE3 "EE] ,2®UCs,Ta
Fig. 8. Geological map of the Zhovtianski pegmatite field:
1-4 - formation of Kryvorizka series: 1 - dolomite, quartz-biotite rock mass with graphite of microschist, diopside quartzites, actinolite shales; 2 - magnetite-hematite jaspilite, magnetite-hematite hornfels; 3 - rock mass of amphibole, mice, mice-amphibole shales; 4 - sericitic quartzite with fuchsite, amphibole-biotite gneiss; 5 - amphibolites of Konkska series; 6 - Demurivski granites; 6 -Dnipropetrovsk plagiomigmatites; 8 - pegmatites; 9 - fractures; 10 - geological boundaries; 11 - notional boundaries of Zhovtianski field of rare metal pegmatites; 12 - Zhovtianski ore occurrence of rare metals.
oid formations of the Dnipropetrovsk complex, which indicates their genetic connection with this complex, as well as their ultrametamorphic nature.
In the second stage within granite-gneiss domes there formed large fields of ceramic pegmatites as derivatives of buried plagiogranite pegmatites (the most well-known are the Bazavlutske pegmatite fields located in the central part of the Saksaganski dome).
Pegmatite formation of the third period is associated with the establishment of greenstone structures and the Kryvorizko-Kremenchutska structural-facial areas. Pegmatite formation is associated with the formation of multi-stage intrusives of two-feldspar
granite complexes (Demurski, Mokromoskivski, To-kivski, Orilski massifs) and was accompanied by the intrusion and inflow of a considerable mass of pegmatite matter into weakened areas of trough greenstone structures with the formation of pegmatites of different types, in particular rare metal and rare earth depending on the time, the depth of its separation and specialization of the massifs themselves. The absence of pegmatite fields within the majority of greenstone structures is explained by only one reason - insignificant erosional truncation of these structures. The fields of rare earth pegmatites are discovered within the Kryvorizko-Kremenchutska structural-facial ar-
eas where they form the Petrovske and Mykolaivske long fields. Pegmatite fields of rare metal specialization (Zhovtovodske, Komendantivske, Mokromos-kovske) are traditionally "attached" to separate greenstone trough structures and their aureole. Grouping with fields of rare earth specialization, they form the long (up to several hundred kilometers) Komendan-tivsko-Zhovtovodsko-Morkomoskovski pegmatite belt. Here are manifested such ore occurrences of rare metals as Komendantivske (Fig.7) and Zhovtovodske (Fig.8) (Isakov, 2013). The fields are formed by the following types of pegmatites: microcline, oligoclase-microcline, oligoclase; albite rare metal: 1) without lithium minerals; 2) with lithium minerals.
Ingulska and Volynska megastructures. The key structural-geological position in the structure of these megablocks is taken by thick granitoid batholites of complex internal structure and wide range of composition. Analysis of the restored sequence of geological processes causing their formation gives an opportunity to regard these megablocks based on the hypothesis of abyssal convection current and magmatic plumes (Isakov, 2017).
In the formation of Ingulska megastructure the following tightly connected structural unites are involved: 1) the Novoukrainski and Korsun-Novomyr-gorodski plutons (magmatic dome); 2) the system of synclinore structures (Bratska and Pryingulska),
Fig. 9 Contour map of Ingulski pegmatite region
1. Small-dome structure of the Bratski and Pryingulski synclinore formed by rock formations of the Ingulo-Inguletska series and granites of the Kirovograd complex. 2. Intrusive formations of the Novoukrainski complex. 3. Intrusive formations of the Korsun-Novomyrgorodski complex. 4. Metaterrigenous formations of the Kryvorika series. 5. Geological boundaries. 6. Fractures. 7. Notional contours of the Bratski pegmatite belt. 8. Notional contours of rare metal pegmatite fields: 1-Vys, 2-Mostove, 3-Lypniazke, 5-Kirovo-gradske. 9. Notional contour of anticipated contour of development of pegmatite fields of chamber pegmatites: 4-notionally contoured Korsun-Novomyrgorodske field. 10. Notional contour of anticipated development of rare metal pegmatite fields. 11. Ore occurrences and deposits of rare metal pegmatites: 1-Mostove, 2-Polohivske, 3-Lypniazke, 4-Stankuvatske, 5-Nadia.
their fringing; 3) Golovanivska and Kryvorizko-Kre-menchutska inclining (suture, according to (Isakov, 2017)) zones fringing the megablock (Fig.9).
Within the Bolynska megastructure tightly connected structural units are singled out : 1) Gorognyts-ko-Korostenski ultrametamorphic magmatic dome (Gorodnytsko-Yemilchynski granite-migmatite dome and Korostenski pluton); 2) the system of synclinore structures forming the Pivdennovolynski synclinore (Teterivski dip, after V.A. Riabenko, or the Zhyto-myrski synclinore, after V.M. Klochkov); 3) Ovrutska graben-synclinal with its Bilokorovytski and Vilchan-ski branches (Fig.10).
The process of granite and pegmatite formation as the main generator of pegmatite matter within megablocks was rather similar and realized in at least three stages.
The first stage is the formation of proper ceramic pegmatites of quartz-oligoclase microcline, quartz-oligoclase, quartz-microcline composition among old ultrametamorphic rock complexes of dome structures (Sheremetivski and Inguletski complexes).
The second stage. The first sub-stage is bedding of granites of Kirovogradski and Zhytomyrski complexes presented by biotite, garnet-biotite, musco-vite-biotite two-feldspar granites, aplite-pegmatoid
Fig. 10 Contour map of Volynski pegmatite region.
1 - migmatites and granites of the Pobuzki complex; 2 - migmatites of the Sheremetivski and Tetiivski complexes; 3 -
rock complexes of the Rosynsko-Tikytska series; 4 - rock of Teterivska series complex; 5 - granites of Zhytomyrski complex;
intrusive formations of complex (6 - gabbro, 7 - granite); 8 - rock of Ovrutska series complex; 9 - granites of Perzhanski complex; 10 - notional contour of Volynski pegmatite belt; 11 - notional contour of Korostanski stockwork of chamber pegmatites;
12 - notional boundaries of pegmatite fields: a - rare metal and rare earth; b - chamber; c - ceramic; 13 - Pegmatite fields:
a - rare metal pegmatites: 1 - Gorodnitske; 2 - Koretske; 3 - Shepytivske; 4 - Polonno-Baranivske; 5 - Novograd-Volynske;
6 - Serbivske; 7 - Barashenske; 8 - Tesnivske; 9 - Kodynynske; 10 - Berdychivske; 11 - Zhytomyrske; 12 - Kocherivske; b -chamber pegmatites: 13 - Ignatpilske; 14 - Behinske; 15 - Volodarsko-Volynske; 16 - Irshanske; 17 - Malynske; c - ceramic pegmatites: 18 - Yablunovsko-Volodymyrske.
granites, aplites and pegmatites that form a range of massifs within synclinore structures, including rather large ones. Their age is estimated at 2 000 mln years and older (Shcherbak,2005). These granite complexes are associated with the majority of ceramic, rare earth and rare metal pegmatites. The absence or low occurrence of rare metal pegmatites within the Volynska megastructure can be explained only by its insignificant erosive level. This didn't allow us to sort out these pegmatite fields, and in the given scheme (Fig. 10) all of them are highlighted as potentially rare metal fields.
The second sub-stage is a further formation of central magmatic dome and bedding of two large massifs (plutons) of complex structural and material composition within the Ingulski megablock: Novoukrainski and Chygyrynski plutons composed mainly by granites of biotite and granite-biotite with bodies of gab-bronorite, norites, monzodiorite, monzonite, quartz syenite of frequent occurrence. The age of rock formations of the Novoukrainski complex is estimated at 2030 - 2000 Ma (Shcherbak, 2005), that is the granites of the Kirovogradski complex and associated granites
1EZI »IZ2I эЕЭ eL3 'Ö
0 330 660 990 m
1_I_I_I_I
Fig. 11 Schematic formation of Stankuvatski and Nadia nodes of rare metal pegmatites.
1 - gneiss and shale of biotite, garnet-biotite, cordierite-biotite, graphite-cordierite-biotite, amphibol-biotite, pyroxene-biotite nature;
2 - amphibolites; 3- biotite granites with garnet and cordierite; 4 - pegmatites: petalite-spodumene, albite rare metal; 5 - quartz two-feldspar ceramic pegmatites; 6 - geological boundaries; 7 - cross-section line.
and aplites are derivates of a common magmatic environment that were separated at the early abyssal stage of its establishment, which after some period of time were moved and formed the Novoukrainski and associate massifs. Thus, pegmatites within the Ingulska megastructure (rare metal ones in particular) associated with both the Kirovogradski and Novoukrainski granite complexes have common genetic nature and are divided by the formation stages. This complex is associated with pegmatites of the Polohivske deposit of petalite pegmatites, the Lipniazhska group of de-
posits (Stankuvatske, Nadia, Lipniazhske) (Fig. 11) and Mostova group of deposits (Mostove-3, in particular) (Fig. 12) of rare metal pegmatites (Voznyak, 2001, Yeryomenko, 1996, Ivanov, 2002).
The third stage is the final stage of formation of the central magmatic dome - bedding of the Korsun-Novomyrgorodski and Korostenski plutons of complex structural and material composition formed by mainly granites of rapakivia and gabbro-anorthosite. Granites of these plutons are also associated with pegmatites, chamber ones in particular (known Volynska
Fig.12 Scheme of formation of Mostove-3 pegmatite node 1 - Biotite-gneiss; 2 - Biotite gneiss with silimonite, cordierite, muscovite, garnet; 3 - Quartz-albite rare metal pegmatites; 4 - Quartz two-feldspar pegmatites.
group of deposits of chamber pegmatites (Mineralogy, 1973). Their absence or insignificant occurrence within the Ingulska megastructure can be explained by the significant erosive level of the massif, which resulted in the destruction of the majority of chamber pegmatites.
Thus, within the Ingulska and Volynska mega-structures we observe such pegmatites that both in common and separately form independent pegmatite fields: proper ceramic, rare earth and rare metal, as well as chamber pegmatites. The time sequence of the formation of the indicated types of pegmatites appears as follows: ceramic pegmatites ^ rare earth and accompanying barren pegmatites ^ rare metal and accompanying barren pegmatites ^ chamber pegmatites
Systematization of pegmatites of the Ukrainian Shield. Pegmatites are not original or unique either for the Ukrainian Shield or for other Early Pre-Cambrian structures of the world. This is explained, first of all, by geological and structural conditions of this period that were favourable for the development of different types of granitoid formations which, in their turn, were the main generators of pegmatite matter not only in early but also in later periods of earth crust development. Different depth of origin and establishment of magmatic environments and variety of forms of granitoid manifestations in their turn gave origin to the variety of forms, composition, geochemistry, metallogenic specialization of pegmatites. Their form, composition, geochemical and metallogenic specialization were also greatly influenced by Pt-con-dition of the surrounding environment, composition of the hosted rocks, tectonic conditions and a range of other factors occurring in the process of their establishment and formation. All the above conditioned significant differences of pegmatites in composition of both basic rock-forming mineral and in internal structural and texture characteristics, as well as in microelement composition and the presence of a large range of accessory and rare minerals that reach percentage composition in pegmatites or become rock-forming. This characteristic of formation and internal structure, as well as the composition of pegmatites resulted in the appearance of different, often opposite, working hypotheses about their genesis and formation (Ginzburg, 1979, Kuz'menko, 1978, Nikanorov, 1979, Petrov, 1975, Shavlo, 1984, Shmakin, 1987 and oth.). For instance, O. Fersman and K. Vlasov considered pegmatites to be the result of the crystallization process of residual magmatic melting enriched by volatile components; while D. Korzhynski and V. Nikitin thought it to be the result of influence of
post-magmatic melting on re-crystallization and replacement of magmatic genesis rocks. This, in its turn, caused a large number of classification systems and classifications developed by different authors in different years. The majority of these classifications are built on classification features - typomorphic, rock-forming and ore minerals, structural and textural characteristics of pegmatites, abyssal establishing, or economic value.
Sometimes classification systems are composed by a range of genetic and geological-structural features and conditions of pegmatite formation. The principles of their classification are acceptable with one provision: the desire of these authors to build the general holistic concept of singling out pegmatites by the primary characteristic (gradual change of depth or the level of regional metamorphism, processes of re-crystallization and replacement during metamor-phism and metasomatosis, rare metal mineralogical and geochemical specialization etc) resulted in significant simplification of the process of formation and establishment of pegmatites of different associations, as well as in the loss of a range of important factors of this process. That is, the role of separate and, in the authors' opinion, major and only factors in the establishment of pegmatite associations is not so significant and in many cases exaggerated.
Without going deep into general critical analysis, for it is already presented in the above mentioned researchers and authors in (Isakov, 2006), on the basis of genetic and geological-structural factors of formation of pegmatites of the Ukrainian Shield , we will try to construct a general scheme that would reflect general regularities of pegmatite formation in early Pre-Cam-brian structures and would reconstruct the general logical chain of abyssal processes of their formation (Table 1). It is based on the characteristic features of formation and development of pegmatite-generating environments and pegmatite-bearing structures, tectonic-structural characteristics of pegmatite-bearing areas during the process of their establishment, as well as the influence of external metamorphogenic-metasomatic processes on the already formed pegmatites.
By the development of pegmatite-generating environments we single out:
- three genetic groups of pegmatites: ultrameta-morphogenic, magmatogenic and metamorphogenic-metasomatic;
- six genetic sub-groups of pegmatites: migma-tite; autochtonous granite massifs; metamorphogenic and metasomatically replaced and formed pegmatites; multi-phase intrusive granite massifs; multi-phase in-
Table 1. Classification of pegmatites of Pre-Cambrian shields (on the example of the Ukrainian Shield)
Groups of pegmatites Genetic Associations Types of pegmatites
subgroups of pegmatites (formations) of pegmatites
Genetic Geological-structural Mineralogical (by ore-formation minerals) Geochemical-metallogenic
Subgroups
Miarolitic and By different classifications offered by M.P.Yermakov
chamber pegmatites (1957) and Ye.K.Lazarenko, V.I.Pavlyshyn (1973)
Multi-phase granite batholiths
s £ lo Rare-metal pegmatites Microcline Microcline-albite Microcline-albite and Rare metal, ore specialization in Li, Rb, Cs, Ta, Nb, Be, Sn
ht ta spodumene
s e r d M e S Ceramic pegmatites Microcline Microcline-oligoclase Rare geochemical and insignificant rare specialization in Nb
c ■g rut c ucrt s - e euml pl h ghu d e vi is I e sf sru is ei m se sha neil Thorium-rare-earth pegmatites Albite-amazonite Microcline Albite-microcline Albite-quartz Oligoclase-microcline Rare earth, ore specialization in TR, Y, Ta, Nb, Zr
« M o "Ss S o rt - e em 1 * Ceramic pegmatites Microcline Microcline-oligoclase Barren;
M ga do ddn Microcline-spodumene
M na aer o noil lc n ys s e O urst se Rare-metal pegmatites Albite-spodumene Albite-petalite-spodumene Albite Albite-microcline Rare metal and ore specialization in Li, Rb, Cs, Ta, Nb, Be, Sn
- e em o Q gh neo Multi-phase intrusive granite massifs Microcline
o a * § d ts n s a " or rg ng il n Rare-metal muscovite-feldspar pegmatites Muscovite-albite-micro- cline-oligoclase Muscovite-microcline-oli-goclase Rare metal,geochemical and ore specialization in Ta, Nb, Be, Li, Rb, Cs
s lc Muscovite-feldspar Muscovite-microcline- Barren, possible (?) geo-
S "H od a pegmatites oligoclase Muscovite-oligoclase chemical specialization in Nb, Zr, TR, U
1 Ceramic pegmatites Microcline Microcline-oligoclase Ditto
Beryl-muscovite Muscovite-albite-micro- Beryl-bearing, geochemical
o ta am o c is H M o g etc rts tf O o pegmatites cline-oligoclase Muscovite-oligoclase specialization in Be, Nb, Zr, TR, U, ore specialization In Be
e ci ne Muscovite Muscovite- microcline- Barren, possible (?) geo-
s - c cin 1) & 8 M N pegmatites oligoclase Muscovite-oligoclase chemical specialization in Nb, Zr, TR, U
M o h phr o te eM s seurt c 3 ts la s ne io em Metamorpho-genic-metaso-matic replaced and formed pegmatites Ceramic pegmatites Microcline Microcline-oligoclase Barren, possible (?) geo-chemical specialization in Nb, Zr, TR, U
Ultra-metamorpho-genic g -6 sd sn ie a fl M - et tinar Autochthonous granite massifs Ceramic pegmatites Oligoclase Microcline-oligoclase Microcline Albite- microcline-oligo-clase Barren; Ceramic raw material; geochemical specialization in Nb, Zr, TR, U
d Migmatite
trusive alkaline massifs; multi-phase granite batho-lites.
By the nature of pegmatite-bearing structures, we distinguish the following structural groups: granite-gneiss regional structures and domes; dome-synclinore and dome-trough plume-structures (subgroups: intradome synclinore and trough, in particular greenstone structures; intrusive domes and batho-lites); specific tectonic zones of stress.
Associations (according to (Ginzburg, 1979) -formations) and mineralogical-geochemical and ore types of pegmatites are singled out after (Ginzburg, 1979, Kuz'menko, 1978, Nikanorov, 1979, Petrov, 1975, Shavlo, 1984, Shmakin, 1987and others) on the basis of characteristic mineralogical and geochemical features of pegmatites.
The offered scheme is rather cumbersome; however it allows us to present gradual development of pegmatite formation with the change of associations and types of pegmatites in the full tectonic-magmatic cycle of megastructure formation, as well as the development of the pegmatite process in one range of pegmatite associations connected with the development of granitoid process within megastructures (ceramic pegmatites ^ uranium-rare earth ^ rare metal ^ thoria-rare earth ^-miarolitic and chamber pegmatites) and ranges of types of pegmatites associated with the development of pegmatite associations during one period of megastructure establishment.
Wesingleoutaseparategroupofmetamorphogenic-metasomatic pegmatites spread within specific tectonic zones of stress (pressure structures in edge zones of shields and zones of tectonic-metamorphic activization of granite-gneiss domes and others) and composed of formations of muscovite and beryl-muscovite pegmatites. These pegmatites within the Ukrainian Shield, in our opinion, are not revealed, as those pegmatites with high (up to 30%) content of muscovite (Mokromoskovske pegmatite field), that we personally researched, are obviously primary unchanged rocks with abnormal content of muscovite that formed during crystallization in the closed system of pegmatite vein separated from parent massif.
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