State Geological Map of Ukraine

MINISTRY OF ENVIRONMENT PROTECTION OF UKRAINE STATE GEOLOGICAL SURVEY

NORTHERN STATE REGIONAL GEOLOGICAL ENTERPRISE "PIVNICHGEOLOGIA"

STATE GEOLOGICAL MAP OF UKRAINE

Scale 1:200 000

CENTRAL-UKRAINIAN SERIES Map Sheet M-35-XXII (STAROKOSTYANTYNIV)

EXPLANATORY NOTES

Compiled by: V.V.Lukash (responsible executive), E.V.Gadyuchka, O.G.Lisnyak, G.G.Vynogradov, K.M.Perelygin, Z.P.Okhynko, N.K.Grytsenko, L.V.Bedrak, A.V.Fedorov

Editors: A.S.Voynovskiy, S.S.Derkach

Expert of Scientific-Editorial Council: P.F.Bratslavskiy (UkrSGRI)

English Translation (2010): B.I.Malyuk

Kyiv - 2007 (2010)

UDC [560.81/.82 + 502.51/.53] (477.41-37) + (477.45/46-37)

The State Geological Map of Ukraine in the scale 1:200 000, map sheet M-35-XXII (Starokostyantyniv). Explanatory Notes. Kyiv: State Geological Survey, Northern State Regional Geological Enterprise "Pivnichgeologia", 2007. – English translation. – Kyiv: UkrSGRI, 2010. – 171 p.

Authors:

V.V.Lukash (responsible executive), E.V.Gadyuchka, O.G.Lisnyak, G.G.Vynogradov, K.M.Perelygin, Z.P.Okhynko, N.K.Grytsenko, L.V.Bedrak, A.V.Fedorov

Editors:

A.S.Voynovskiy, Candidate of Geological-Mineralogical Sciences, S.S.Derkach

Expert of Scientific-Editorial Council

P.F.Bratslavskiy, Ordinary Scientist, UkrSGRI

English translation (2010)

B.I.Malyuk, Doctor Hab. of Geological-Mineralogical Sciences, UkrSGRI

In the explanatory notes geological data are summarized obtained after previously published edition of the medium-scale maps, updated and systematized in the course of extended geological study in the scale 1:200 000 in the map sheet M-35-XXII (Starokostyantyniv). Description is given for geological map and map of mineral resources of pre-Quaternary units, geological map and map of mineral resources of Quaternary sediments, geological map and map of mineral resources of crystalline basement, geological map of pre- Mesozoic units. The geological column is described from the crystalline base up to modern sediments, tectonic structure, mineral resources, ecological-geological situation in the area. The list of mineral deposits and occurrences is compiled. The work is devoted to the wide range of specialists in geological sciences and natural resources.

CONTENTS

0Abbreviations used in the text...... 1346

1INTRODUCTION...... 1357

21. GEOLOGICAL STUDY DEGREE ...... 1369

3Geological study...... 1379

4Geophysical study ...... 13810

5Hydrogeological study...... 13912

6Ecological study ...... 14012

72. STRATIFIED UNITS ...... 14113

8Archean Eonotheme ...... 14216

9Paleo-Archean Eratheme ...... 14316

10Proterozoic Eonotheme ...... 14427

11Paleo-Proterozoic Eratheme ...... 14527

12Neo-Proterozoic Eratheme ...... 14629

13Vendian System...... 14729

14Mesozoic Eratheme...... 14838

15Cretaceous System...... 14938

16Upper division ...... 15038

17Cenozoic Eratheme ...... 15140

18Paleogene System...... 15240

19Eocene division...... 15340

20Neogene System ...... 15446

21Miocene division ...... 15546

22Pliocene division...... 15651

23Quaternary System ...... 15752

24Pleistocene division ...... 15852

25Holocene division ...... 15959

263. NON-STRATIFIED UNITS ...... 16061

27Intrusive rocks...... 16162

28Archean Eon...... 16262

29Paleo-Archean Era...... 16362

30Proterozoic Eon ...... 16463

31Paleo-Proterozoic Era ...... 16563

32Ultra-metamorphic rocks...... 16679

33Archean Eon...... 16779

34Paleo-Archean Era...... 16879

35Meso-Archean Era...... 16980

36Proterozoic Eon ...... 17082

37Paleo-Proterozoic Era ...... 17182

38Retrograded, hydrothermally-metasomatically and tectonically altered rocks, tectonites ...... 17288

394. WEATHERING CRUST ...... 17390

40Weathering crust of granitoid rocks ...... 17490

41Weathering crust of biotite, garnet-biotite, cordierite-garnet-biotite, graphite-biotite gneisses ...... 17592

42Weathering crust of pyroxene, garnet-pyroxene, amphibole, biotite-amphibole gneisses and mafic gneisses 17692

43Weathering crust of gabbro, gabbro-amphibolites, diabases, gabbro-diabases, monzonites and gabbro-

monzonites, pyroxenites ...... 17792

44Weathering crust of syenites ...... 17893

455. TECTONICS...... 17994

46Lower tectonic level...... 18094

47Tectonic blocks...... 18195

48Tectonic breaks...... 18298

49Upper tectonic level ...... 183102

50Vendian tectonic floor ...... 184102

51Mesozoic tectonic floor ...... 185103

52Cenozoic tectonic floor...... 186103

3 536. HISTORY OF GEOLOGICAL DEVELOPMENT...... 187107

54Archean-Proterozoic stage...... 188107

55Paleo-Archean epoch...... 189107

56Meso-Archean epoch...... 190107

57Neo-Archean – Paleo-Proterozoic epoch...... 191108

58Paleo-Proterozoic epoch ...... 192108

59Vendian stage ...... 193109

60Mesozoic and Cenozoic stages ...... 194110

617. GEOMORPHOLOGY AND RELIEF-FORMING PROCESSES...... 195112

62Northern peri-glacial zone...... 196112

63Central-Ukrainian loess zone...... 197113

64Sluch river valley...... 198115

65South Boug river valley ...... 199116

668. HYDROGEOLOGY ...... 200118

679. MINERAL RESOURCES AND REGULARITIES IN THEIR DISTRIBUTION...... 201126

68Combustible mineral resources ...... 202126

69Solid combustible minerals...... 203126

70Peat ...... 204126

71Metallic mineral resources...... 205127

72Non-ferrous and base metals...... 206127

73Nickel...... 207127

74Titanium...... 208127

75Rare metals ...... 209128

76Molybdenum...... 210128

77Precious metals ...... 211128

78Gold ...... 212128

79Rare-earth metals...... 213128

80Monazite ...... 214128

81Radioactive metals...... 215129

82Uranium, thorium...... 216129

83Non-metallic mineral resources...... 217129

84Ore-chemical raw materials ...... 218129

85Agro-chemical raw materials ...... 219129

86Raw materials for soil chemical improvers...... 220131

87Non-metallic ore raw materials...... 221131

88Electric- and radio-technical raw materials...... 222131

89Adsorption raw materials...... 223131

90Facing stone raw materials (decorative stone) ...... 224132

91Glass and porcelain-faience raw materials...... 225132

92Construction raw materials ...... 226132

93Petrurgy and light concrete filler raw materials ...... 227132

94Construction lime and gypsum raw materials...... 228133

95Quarry-stone (aggregate) raw materials...... 229133

96Brick-tile raw materials...... 230133

97Waters...... 231134

98Groundwaters...... 232134

99Fresh waters ...... 233134

100Mineral waters ...... 234135

101Regularities in distribution of mineral resources...... 235135

102Mineral resources in the rocks of crystalline basement and their weathering crusts ...... 236135

103Metallic mineral resources...... 237135

104Non-metallic mineral resources ...... 238136

105Regularities in distribution of mineral resources in sedimentary cover...... 239137

10610. ASSESSMENT OF THE AREA PERSPECTIVES...... 240139

107Solid combustible minerals ...... 241139

108Peat ...... 242139

109Metallic mineral resources ...... 243139

110Rare metals ...... 244139

4 111Radioactive metals ...... 245139

112Precious metals...... 246139

113Non-metallic mineral resources ...... 247140

114Ore-chemical raw materials...... 248140

115Agro-chemical raw materials...... 249140

116Non-metallic ore raw materials ...... 250140

117Adsorption raw materials...... 251140

118Electric- and radio-technical raw materials ...... 252140

119Facing stone and construction raw materials...... 253140

120Groundwaters...... 254141

12111. ECOLOGICAL-GEOLOGICAL SITUATION...... 255142

122Landscape zonation...... 256144

123Assessment of soil and bottom sediment contamination...... 257145

124Assessment of surface and groundwater contamination ...... 258145

125Assessment of EGP suffering...... 259146

126CONCLUSIONS ...... 260148

127REFERENCES ...... 261150

128Published...... 262150

129Unpublished ...... 263150

130ANNEXES...... 264153

131Annex 1. List of deposits and occurrences indicated in the “Geological map and map of mineral resources

of pre-Quaternary units” of map sheet M-35-XXII (Starokostyantyniv)...... 265153

132Annex 2. List of deposits and occurrences indicated in the “Geological map and map of mineral resources

of Quaternary sediments” of map sheet M-35-XXII (Starokostyantyniv) ...... 266161

133Annex 3. List of deposits and occurrences indicated in the “Geological map and map of mineral resources

of crystalline basement” of map sheet M-35-XXII (Starokostyantyniv) ...... 267165

0Abbreviations used in the text

AC – adsorbing complex of exchange cations Aef. – efficient specific activity of natural radionuclides BCP – bulk contamination parameter Derzhgeolkarta-200 – the State Geological Map in the scale 1:200 000 DGM – Deep Geological Mapping (-50, -200 means in the scale 1:50 000 and 1:200 000 respectively) DH – drill-hole EEP – Eastern-European Platform EGP – exogenic geological processes EGSF-200 – Extended Geological Study of the Fields in the scale 1:200 000 GEE – Geological Exploration Expedition GM-50 – Geological Mapping in the scale 1:50 000 GPM-50 – Geological-Prognostic Mapping in the scale 1:50 000 IGMOF – Institute of Geochemistry, Mineralogy and Ore Formation, UNAS IGS – Institute of Geological Sciences, UNAS IP – Induced Polarization ISC – Inter-Ministry Stratigraphic Committee LTC – Litho-Tectonic Complex LTZ – Litho-Tectonic Zone MZ – Metallogenic Zone NAS - National Academy of Sciences of Ukraine RW-CDP – seismic method of reflected waves and common deep point SCMR – the State Commission on Mineral Reserves SE – State Enterprise SEP – Standard [vertical] Electric Profiling SSU – the State Standard of Ukraine SRGE – State Regional Geological Enterprise TAC – top admissible concentration TAL – top admissible level TMZ – Tectonic-Metallogenic Zone UISC – Ukrainian Inter-Ministry Stratigraphic Committee UkrSGRI – Ukrainian State Geological Research Institute UNAS – National Academy of Sciences of Ukraine UTCMR - Ukrainian Territorial Commission of Mineral Reserves VED – value of exposition dose VPP – Volyno-Podilska Plate

1INTRODUCTION

The map sheet territory M-35-XXII (Starokostyantyniv) is located in Shepetivskiy, Starokostyantynivskiy, Khmelnytskiy, Starosynavskiy, and Letychivskiy areas of Khmelnytska Oblast, Lyubarskiy area of Zhytomyrska Oblast, Khmilnytskiy and Litynskiy areas of Vinnytska Oblast. It is limited by coordinates 27o and 28o E longitude, and 49o20’- 50o00’ N latitude. The map sheet square is 5352 km2. The major towns include Khmeltynskiy, Letychiv, Khmilnyk, Stara Synyava, Starokostyantyniv, Stariy Ostropil, Grytsiv, Lyubar, which are connected one to another by the network of railways and motorways. In the orographic respect most part of the territory is situated within Volyno-Podilska height and comprises hilly plain cut by the river and gully valleys especially in the western and southern parts. The surface altitudes are 250.0-400.0 m. Hill tops are mainly flat and their slope angles – 4-10o. To the north-east from the line Khmilnyk-Starokostyantyniv the cutting degree decreases and the surface becomes wavy. The river and gully valleys are broad, swamped, with flat (up to 5o) slopes. The soils are mainly loam and in the river valleys peated. The groundwater depth is 6-15 m. The hydrographic network is branched enough. The major rivers in the area include South Boug and Sluch. Their river course width is 12-40 m, depth – 0.9-2.0 m, flow speed – 0.1-0.4 m/sec. The courses are often dammed with accompanied big pond formation. The South Boug river basin includes the right branches Vovk and Fosa, and the left ones: Zinchytsya, Buzhok, Ikva. The Sluch river basin includes the right branches: Mshanetska Ruda, Popivka, Taranka, Verbka, and the left ones: Ikopot, Korytnytsya, Stavyska, Derevychka. The territory is situated in the forest-steppe zone. The area climate is moderate-continental with month- average temperature in January -5.3…-5.5oC (minimum temperature -30…-35oC), in July +18.4…+20.0oC (maximum +38.5oC). Annual average amount of precipitates is 540-610 mm. The population density in the area attains 68 persons per 1 km2. The inhabited localities are spaced regularly enough. The biggest ones are Oblast center Khmelnytskiy – 261.6 thousand people; area centers: Starokostyantyniv town – 38.6 thous. people, Khmilnyk – 30.1 thous. people, Letychiv – 12.3 thous. people. The local inhabitants are mainly involved in agriculture production manufacturing and processing. In Khmeltynskiy town the machinery, electronic, construction, woodworking, light and food industries are developed. Khmilnyk, Starokostyantyniv and Letychiv towns are machinery-construction and metal-processing centers, as well as agriculture production processing. Khmilnyk town is known balneology resort with the branch of the Resort and Physiotherapy Institute. The studied area is located in the western part of Ukrainian Shield and its western slope, mainly within Dnistersko-Buzkiy mega-block (according to zonation accepted in the “Chrono-stratigraphic scheme of Early Precambrian in Ukrainian Shield”, Kyiv, 2004), which in the far southern and south-western map sheet parts adjoins Volynskiy mega-block. By geology the area is classified to be closed three-fold one. The territory includes Quaternary and pre-Quaternary (including Vendian rocks in the western part of map sheet) cover complexes and the folded complex of the basement. The complex of geological studies and summary works to the Derzhgeolkarta-200 is conducted by the Mapping group of SE “Pivnichgeologia” under leadership of the group head V.P.Bezvynniy and general supervision by the Director General V.S.Metalidi and Chief Geologist V.L.Prykhodko. Laboratory studies are performed by:  SE “Pivnichgeologia”: spectral semi-quantitative, spectral-gold-metric, mineralogical, lithological, silicate, chemical analysis for specific elements, radio-spectrometry, flame-photometric of alkaline elements;  Pravoberezhna GE of SE “Pivnichgeologia”: spectral semi-quantitative, mineralogical analyses, thin and polished section preparation;  IGMOF: chemical analysis of minerals, X-ray analysis of rare-earth elements, isotopic analysis including absolute age determination;  IGS: palinological, macro- and micro-fauna analyses;  SE “Geoinform Ukrainy” – palinological analysis;  National Mining University (Dnipropetrovsk town) – emission quantometry analysis for platinum- group elements (PGE);  SE “Kirovgeologia” – fine assay for gold and PGE. In the design of Derzhgeolkarta-200 map set materials are used from extended geological study of the field in the scale 1:200 000, preceded the preparation to publication, and geological mapping works in the scale 1:200 000 of N.E.Strelkova, 1960 (GM-200), V.I.Pochtarenko, 1971 (DGM-200); in the scale 1:50 000:

7 Yu.K.Piyar, 1974, L.V.Bochay, 1977, P.F.Bratslavskiy, 1988, B.M.Rybalt, 2003; geological and hydrogeological mapping in the same scale: N.I.Ivanchenko, 1969; hydrogeological and engineering-geological mapping in the scale 1:50 00 by T.V.Klyovana, 1988; as well as prognostic-geological works in the scale 1:100 000 by P.V.Vinnychenko, 1991 and prospecting works for various minerals: V.I.Serzhyn, 1969, D.A.Lavrov, 1963; V.O.Rachenkov, 1967, Yu.G.Gerasimov, 1960, R.M.Dovgan, 2004, P.A.Gnatyuk, 1971, and others. In the course of the works conducted the authors have got assistance and consulting from the officers of the State Geological Survey, UkrSGRI, IGMOF, Kyiv National University: M.V.Geichenko, M.M.Kostenko, A.S.Drannyk, V.Ya.Velikanov, P.F.Bratslavskiy, B.D.Vozgrin, Yu.M.Veklych, V.M.Klochkov, A.M.Ponomarenko, S.G.Kryvdyk, S.Yu.Bortnyk, O.I.Lukienko, V.P.Palienko.

21. GEOLOGICAL STUDY DEGREE

16Geological study

Preliminary geological map in the scale 1:200 000 was designed after results of geological mapping in 1957-1959 conducted under leadership of N.E.Strelkova. The stratigraphic sub-division of sedimentary cover was performed, Paleogene Kyivska Suite and Lower Cambrian (Vendian) sediments were distinguished, wide development of charnockite rocks in the crystalline basement was established, and assumption was made on the tectonic nature of the contact between the crystalline massif and its western slope. From the modern point of view the geological maps are outdated being based on the limited data and stratification in the sedimentary cover is preformed using the schemes and legends which differ from the modern ones. This note also concerns all other works except geological mapping [51]. In 1968-1971 V.I.Pochtarenko [47] had conducted the works on deep geological mapping in the scale 1:200000 over map sheet M-35-XXII (Starokostyantyniv). By the results of works, the detailed enough subdivision of crystalline basement rocks was made for the first time in the given area. The composition, setting and distribution areas of the Upper Precambrian sedimentary-volcanogenic and sedimentary rocks were studied and their stratigraphic subdivision was designed. The Malobratalivskiy and Kovalenkivskiy occurrences of molybdenum mineralization were encountered. The geological mapping in the scale 1:50 000 is performed for most part of the map sheet. The complex geological-hydrogeological mapping in the given scale was conducted in 1965-1969 by M.I.Ivanchenko [28] in the map sheets M-35-92-B,D (northern half). It was accompanied by significant drilling and various sampling. Most important results of these works include: design (for the first time) of geological map for crystalline basement in the scale 1:50 000, adjustment for distribution of previously known crystalline rocks and definition of some new petrographic varieties; distinguishing the series of north-west-trending thick tectonic zones accompanied by radon water deposits and rare-metal and radioactive metal occurrences. In 1972-1974 Yu.K.Piyar [44] had conducted geological mapping in the scale 1:50 000 in the territory of map sheets M-35-80-B,D. For the first time the Middle Sarmatian age of clayey-sandy sediments was confidently determined. Malobratalivskiy and Kovalenkivskiy occurrences of molybdenum mineralization were studied in more details. And three graphite occurrences were encountered nearby Vyshchikusy village. In 1974-1977 L.V.Bochay [13] has conducted geological mapping in the scale 1:50 000 over the territory of map sheets M-35-79-D, -80-A, C. After results of these works Varvarivskiy massif of monzonites and gabbro-monzonites is identified and delineated, and tectonics of the area was adjusted. Graphite, apatite, primary kaoline and claydite occurrences are distinguished. In 1984-1988 P.F.Bratslavskiy [15] had conducted the deep geological mapping in the scale 1:50 000 over the territory of map sheets M-35-80-B,D. By these works, the rocks of Dnistersko-Buzka Series are divided into Tyvrivska and Bereznynska sequences; relation of low-grade molybdenum mineralization with the core portions of granodiorite (charnockite) massifs is established; in the north-eastern limb of Khmelnytska tectonic zone the faults are mapped as the thrusts with the flat-dipping displacement plane. The studies in Malobratalivskiy and other minor molybdenum occurrences continued. Important data on the structure of upper (especially Quaternary) part of sedimentary cover were received from the hydrogeological and engineering-geological mapping in the scale 1:50 000 in the map sheets M-35-80-A,B,D (a,b) [32]. The latest regional geological mapping works in the scale 1:50 000 include the grouped geological mapping in the map sheets M-35-91-D; M-35-92-A,C,D (southern half) conducted in 1989-2002 [51]. Sedimentary cover and basement rock subdivision is made on the ground of modern stratigraphic schemes and legends. For the first time in the studied area the sequence of Sarmatian clays, sands and limestones is divided into three sub-sequences; litho-tectonic zonation is performed for pre-Quaternary sedimentary rocks; the age and structure of South Boug river terrace complexes are adjusted; ultra-metamorphic charnockitoids and granitoids in the area are divided into three complexes: Gayvoronskiy, Litynskiy and Berdychivskiy. New data are obtained concerning the rock composition, absolute age and structure of the massifs of Proskurivskiy complex. In the course of geophysical and geochemical works, preceded to the grouped geological mapping, the Goloskivskiy apatite ore occurrence is distinguished and then preliminary studied during the mapping. Khmelnytska metallogenic zone with specialization for apatite mineralization is distinguished and within this zone – Goloskivske ore field, and Antonivske and Rudnyanske ore-bearing fields are defined.

9 Despite of considerable amount of geological studies (Fig. 1.1), the following unsolved problems were mentioned in the given map sheet before the start of works in the frame of EGSF-200:  Quaternary sediments subdivision by climatic-stratigraphic sub-units taking into account their genetic types and spatial zonation;  stratification of Quaternary sediments in the sedimentary cover over most part of the territory was conducted based on the outdated schemes and confidence of the stratons’ boundaries did not always correspond to the scale of map;  subdivision of granitoids and definition of their affinity to specific complexes was conducted in the northern part of map sheet only [51];  the data on tectonic structure of the area do not match the modern insights. These issues were mainly solved by means of extended studies and these data are taken as the background to the given set of map Derzhgeolkarta-200. Prospecting and exploration works for various minerals were conducted in the map sheet M-35-XXII in different years. In 1960-1963 and 1964-1966 [36, 37] prospecting works for rare metals, feldspar and abrasive (garnet) raw materials were conducted and by these results occurrences and mineralization points of these minerals were distinguished which are not economic at present. In 1964-1967, in the course of prospecting works for brown coal in Upper Pobuzhzhya [48], two paleo- depressions were studied: Vododilna and Khmilnytska. No perspective sites were distinguished in the given map sheet. Kirovske SE in the map sheet territory has conducted specialized prospecting for radioactive raw materials with considerable amount of drilling: in the area of Khmilnyk town in 1956-1960 [21] and in 1969 [46]; along the western slope of Ukrainian Shield in 1982-1986 [16] and in 1985-1997 [17]. Some occurrences and mineralization points of radioactive metals were encountered. In 1986 prospecting works for the hard-rock source regions for diamonds were conducted in the central and western parts of Ukrainian Shield [39], and Pravoberezhna GE of SE “Pivnichgeologia” continues these works in Berdychivske uplift [23] which encompasses the south-eastern part of the map sheet. In 1988-1994, in the course of prospecting for nickel in Krasnogorsko-Zhytomyrska zone in the map sheet area, Varvarivskiy massif of mafic and ultramafic rocks was studied in details [20] and perspectives for discovery of sulphide copper-nickel mineralization over there were examined.

17Geophysical study

The systematic geophysical surveys over map sheet area were commenced in the first half of 50th of XX century and these works accompanied the geological prospecting for nickel. In 1952 the Aero-geophysical group of UGU over entire map sheet M-35-XXII the aero-magnetic survey in the scale 1:200 000 was conducted for the first time [55]. These data had allowed definition of general tectonic features of the area and distribution of major rock complexes. In 1957-1959 Volynska geophysical group [45] had conducted gravity survey in the scale 1:200 000 over entire north-western part of Ukrainian Shield resulted in the designed gravity map with iso-anomal lag 2mGal and tectonic sketch of the area in the scale 1:500 000. The first surface magnetic survey in the scale 1:50 000 (500 by 100 m) in the north-eastern part of the map sheet has been conducted by Shepetivska geophysical group [26]. As a result, the map of iso-dynams Za is designed in the scale 1:50 000 coupled with the Za and Vxz plots, the rock systematics was performed by their physical properties, and geological-petrographic map of Precambrian was compiled. In 1958 Vinnytska geophysical group [34] has conducted magnetic survey by grid 500×100 m in the south-eastern part of the territory. The map iso-dynams Za is designed in the scale 1:50 000 with lag 100  and some anomalies distinguished which, according to authors, are caused by Archean metamorphic rocks. Further geophysical studied have been conducted by Yatranska and Volynska geophysical groups, Aero-geophysical group KGKE, group No. 49 of Kirovske SE, seismic group 16/73 of Institute of Geophysics, UNAS, and other scientific and operating teams. The map sheet M-35-XXII is almost completely covered by the conditional geophysical surveys: gravity in the scale 1:50 000 (81%) and 1:200 000 (19%); magnetic (aero-magnetic) in the scale 1:25 000 – 1:50 000 (97%, and 3% by aero-magnetic survey in the scale 1:200 000) and electric VP in the scale 1:200 000 – 1:100 000.

15 3

13 7

8 10

11 9

2 12 1 5 12 14 6

132 4 5678

91110 12 1314 15

Fig. 1.1. Scheme of geological study degree of the map sheet M-35-XXII territory.

Geological mapping in the scale 1:200 000: 1 – N.E.Strelkova, 1960. Geological-hydrogeological mapping in the scale 1:50 000: 2 – M.I.Ivanchenko, 1969. Geological mapping in the scale 1:50 000: 3 – Yu.K.Piyar, 1974; 4 – L.V.Bochay, 1977; 5 – B.M.Rybalt, 2001. Deep geological mapping in the scale 1:200 000: 6 – V.I.Pochtarenko, 1971. Deep geological mapping in the scale 1:50 000: 7 – P.F.Bratslavskiy, 1988. Hydrogeological and engineering-geological mapping in the scale 1:50 000: 8 – T.V.Klyovana, 1988. Prospecting works: for brown coal: 9 – V.O.Rachenkov, 1967; for uranium: 10 – Yu.G.Gerasimov, 1960; 11 – Yu.P.Vinnychenko, 1982-1986 and 1985-1991; for phosphate raw materials: 12 – A.P.Yurchyshyn, 1985-1989 and 1989-1991; for diamonds: 13 – R.M.Dovgan, 2004-2005; for rare metals, feldspar and abrasive raw materials: 14 – D.A.Lavrov, 1960-1963 and 1964-1966; for nickel: 15 – B.L.Vysotskiy, 1994.

18Hydrogeological study

The State Hydrogeological Map of USSR of amp sheet M-35-XXII was created on results of the complex geological mapping in the scale 1:200 000 (including hydrogeological works, specifically, hydrogeological drilling) conducted in 1959-1960 by N.E.Strelkova, A.N.Denysevych and B.Ya.Volovnyk [54] (published in 1974). Since 1964 to 1993 the works were conducted concerning water supplying for the towns and semi-town villages: Khmelnytskiy [49], Khmilnyk [27, 50], Stara Synyava [553], Lyubar [34], Letychiv [35]. Besides that, detailed exploration was conducted in Khmilnytske deposit of mineral radon waters [42, 43].

19Ecological study

In 1982 the study of exogenic geological processes (EGP) is conducted in the territory of Khmelnytska and Vinnytska oblasts in the scale 1:200 000 [33]. As a result, the sources of EGP are identified and mapped, and the engineering-geological zonation of territory is designed. Ecological-geological studies have accompanied the group geological mapping in the scale 1:50 000 in the territory of map sheets M-35-91-D, 92-A,B,D (southern half). The ecological state of geological environment is assessed in the studied area based mainly on the results of own studies [51]. In 2003 O.M.Lepilin [38] has conducted the works on radiation-hygienic evaluation in the deposits of construction and facing raw materials.

32. STRATIFIED UNITS

The column in the given territory includes stratified units in the high-folded crystalline basement, which in the western part of the map sheet are overlain by Vendian sediments (with angular unconformity) and throughout developed Phanerozoic rocks (almost horizontally laying). Neogene and Paleogene sediments are grouped in Berdychivska and Khmelnytska LTZs. Lower Vendian rocks are distinguished in Pivdenno-Buzka and Khomorska LTZs. Precambrian rocks are grouped in two mega-blocks: Volynskiy and Dnistersko-Buzkiy, with definition of Novograd-Volynska and Podilska LTZs respectively. The stratigraphic subdivision of the rocks in territory is performed in accordance with the “Stratigraphic schemes…” (1993), “Correlation chrono-stratigraphic scheme…” (2004), the legend to the series, and matching requirements of the “Stratigraphic Code of Ukraine” (1997) and “Petrographic Code of Ukraine” (1999).

PHANEROZOIC Cenozoic Eratheme Quaternary System Holocene division /H/ eH – eluvial sediments aH – alluvial sediments of flood-lands and gullies lbH – lake-swamp sediments vH – aeolian sediments tH – technogenic sediments bH – biogenic sediments

Pleistocene – Holocene divisions Upper Neo-Pleistocene branch – Holocene division adPIII-H – alluvial-deluvial sediments of gully bottoms dPIII-H – deluvial sediments of gully slopes

Pleistocene Division Neo-Pleistocene section Upper branch vd,ePIII – aeolian-deluvial and eluvial sediments aPIIIvl-ds – Vilshanskiy-Desnyanskiy ledges. Alluvial sediments of the first-second over-flood terraces Buzkiy-Prychornomorskiy climatoliths vd,ePIIIbg-pč – aeolian-deluvial and eluvial sediments dv,ePIIIbg-pč – deluvial-aeolian and eluvial sediments dv,ePIIIvt-pč – Vytachivskiy-Prychornomorskiy climatoliths. Deluvial-aeolian and eluvial sediments vdPIIIpč – Prychornomorskiy climatoliths. Aeolian-deluvial sediments edPIIIdf – Dofinivskiy climatolith. Eluvial-deluvial sediments vdPIIIbg – Buzkiy climatoliths. Aeolian-deluvial sediments edPIIIvt – Vytachivskiy climatolith. Eluvial-deluvial sediments vdPIIIud – Udayskiy climatolith. Aeolian-deluvial sediments edPIIIpl – Prylutskiy climatolith. Eluvial-deluvial sediments

Middle-Upper branches vd,ePII-III – aeolian-deluvial and eluvial sediments dv,ePII-IIIkd-pč – Kaydatskiy-Prychornomorskiy climatoliths. Deluvial-aeolian and eluvial sediments edPII-IIIkd-vt – Kaydatskiy-Vytachivskiy climatoliths. Eluvial-deluvial sediments aPII-IIIčr-tb – Cherkaskiy-Trubizkiy ledges. Alluvial sediments of the third-fourth over-flood terraces

Middle branch vdPIIts – Tyasminskiy climatolith. Aeolian-deluvial sediments edPIIkd – Kaydatskiy climatolith. Eluvial-deluvial sediments Dniprovskiy climatolith vdPIIdn – aeolian-deluvial sediments afPIIdn – alluvial-fluvio-glacial sediments f,lgPIIdn – water-glacial and lake-glacial sediments edPIIzv – Zavadivskiy climatolith. Eluvial-deluvial sediments

Lower-Middle branches e,vdPI-IIsh-zv – Shyrokynskiy-Zavadivskiy climatolith. Eluvial and aeolian-deluvial sediments aPI-IIkn-hd – Krukenytskiy-Khadzhybeyskiy ledges. Alluvial sediments of the fifth-sixth over-flood terraces

Lower branch vdPItl – Tyligulskiy climatolith. Aeolian-deluvial sediments edPIlb – Lubenskiy climatolith. Eluvial-deluvial sediments vdPIsl – Sulskiy climatolith. Aeolian-deluvial sediments edPImr – Martonoskiy climatolith. Eluvial-deluvial sediments aPIbk – Budatskiy ledge. Alluvial sediments vdPIpr – Pryazovskiy climatolith. Aeolian-deluvial sediments edPIsh – Shyrokynskiy climatolith. Eluvial-deluvial sediments

Eo-Pleistocene – Neo-Pleistocene sections Eo-Pleistocene section – Lower branch of Neo-Pleistocene section vd,eE-PI – Aeolian-deluvial and eluvial sediments

Eo-Pleistocene section Upper branch vdEIIil – Illichivskiy climatolith. Aeolian-deluvial sediments edEIIkr – Kryzhanivskiy climatolith. Eluvial-deluvial sediments

Lower branch vdEIbr – Berezanskiy climatolith. Aeolian-deluvial sediments

Neogene System Pliocene division

N1čb - sequence of red-brown clays

Miocene division

Khmelnytska LTZ Berdychivska LTZ N1sg – sequence of parti-colored clays Sarmatian regio-stage N1gp – sequence of clays, sands and aleurolites N1v – sequence of limestones N1vp – sequence of coaliferous sands and clays Poltavska Series N1pd – Podilska Suite N1np – Novopetrivska Suite

Paleogene System Eocene division

Kharkivska Series P2ob - Obukhivska Suite Buchatskiy regio-stage P2kv - Kyivska Suite P2bč - Buchatska Series

Mesozoic Eratheme Cretaceous System Upper division

K2oz – Ozarynetska Suite K2pl – Pylypchanska Suite

Proterozoic Eonotheme Neo-Proterozoic Eratheme Vendian System Upper division Redkinskiy horizon

Mogyliv-Podilska Series

V2mp - Mogyliv-Podilska Series V2jr - Yaryshivska Suite V2br - Bronnytski layers V2bn - Bernashivski layers V2mg - Mogylivska Suite V2ld - Lyadivski layers V2jm - Yampilski layers V2lm - Lomozivski layers V2ol - Olchedaivski layers

Lower division Laplandian horizon

V1vl - Volynska Series Pivdennobuzka LTZ Khomorska LTZ V1gr - Grushkynska Suite V1sl - Slutska Suite V1vn - Vinkivetski layers V1kr - Krasylivski layers V1nv - Novoselski layers V1pg - Prygorynska Suite V1bh - Bakhtynski layers V1bb - Babynski layers V1hm - Khomorski layers

Proterozoic Eonotheme

Podilska LTZ Novograd-Volynska LTZ Teterivska Series PR1vs(?) - Vasylivska Suite

Archean Eonotheme Paleo-Archean Eratheme

Dnistersko-Buzka Series AR1db - undivided rocks AR1br - Bereznynska sequence AR1tv - Tyvrivska sequence

PRECAMBRIAN

20Archean Eonotheme

54Paleo-Archean Eratheme

Podilska LTZ

Dnistersko-Buzka Series

Paleo-Archean Dnistersko-Buzka Series includes all supra-crustal rocks developed in Podilska LTZ of Dnistersko-Buzkiy mega-block and, quite possible, in pre-Paleo-Proterozoic basement of Novograd-Volynska LTZ of Volynskiy mega-block. Based on performed studies and previous data, on the ground of correlation with basic sections of Dnistersko-Buzkiy area they are divided in two sequences: the lower Tyvrivska (AR1tv) and apparently upper Bereznynska (AR1br). The sites, which correspond to the Series rocks by the patterns in physical fields but are weakly studied or underwent essential retrograde alteration while their correlation to the stratotypes of aforementioned sequence is complicated, are mapped as undivided rocks of Dnistersko-Buzka Series (AR1db). The Series rocks are normally developed in minor scialites of various sizes within granitoid rocks, rarely – in the bodies of considerable size which are thought to be the fields of predominant development of supra-crustal rocks in association with granitoids. The Series rocks are metamorphosed under granulite facies conditions, they underwent ultra- metamorphic re-working with three granitization stages, retrograded, metasomatically and dynamo- metamorphically altered in the zones of tectonic breaks. Granitization degree and its thermo-baric conditions have significantly affected variations in the rock chemical and mineral composition, their structures and textures. Under these conditions deciphering of the rock primary composition, column structure and relationships between its constituents is quite complicated. Despite of this, however, definition of two rock associations which correspond to the mentioned sequences is well supported by the complex of petrological, tectonic and geophysical features. Relationships between Tyvrivska and Bereznynska sequences are not confidently identified.

Tyvrivska sequence (AR1tv)

This unit includes the Series portion composed of mainly pyroxene as well as biotite-pyroxene, amphibole-pyroxene mafic gneisses and granite-gneisses, garnet-biotite gneisses with pyroxene, in places with graphite, sillimanite, and with calciphyre and leucocratic granulite interbeds. Mafic gneisses in the column constitute thick bodies and most developed in the batches in comparison with other rocks. The Sequence rocks are preserved in the remnants within charnockitoids of Gayvoronskiy and Litynskiy complexes, as well as younger granitoids. The biggest fields of the Sequence are located in the antiform structures: Medzhybizkiy, Litynskiy and Berdychivskiy domes. The Sequence contains minor bodies of mafic- ultramafic rocks of Sabarivskiy complex. The Sequence rock bodies, considerable in size, are intersected by drill-holes at Verbkivska, Goloskivska and Kovalenkivska sites. The Sequence columns at these sites considerably differ one from another. Comparing these columns with the Sequence columns in adjacent territories, one may conclude that Goloskivskiy column does correspond to its lower portions whereas Verbkivskiy and Kovalenkivskiy ones – to the higher layers. At Goloskivska site two-pyroxene mafic gneisses in association with enderbites of Gayvoronskiy complex predominate. These rocks are cut by gabbroids of Proskurivskiy complex. The most completed column is intersected in DH 1805 (from bottom to top):

1. Biotite-pyroxene enderbite 1.5 m Two-pyroxene amphibolized sheared mafic gneiss. Composition: plagioclase – 60-65%, 2. clinopyroxene – 5-6%, orthopyroxene – 12-15%, hornblende – 12-15%, quartz – single 9.5 m grains, ore minerals – 2-3% 3. Amphibole-pyroxene enderbite 7.3 m

16 Two-pyroxene, dark-greenish-grey, silicified mafic gneiss with enderbite-pegmatite enclaves. 4. Mafic gneiss composition: plagioclase – 50-55%, clinopyroxene – 12-15%, orthopyroxene – 12.1 m 18-20%, biotite – 2-3%, quartz – 5-6%, ore minerals – 3-4% Two-pyroxene, dark-grey with greenish shade, granitized mafic gneiss, in places with enderbite-pegmatite enclaves. Mafic gneiss composition: plagioclase – 50-55%, 5. 6.1 m clinopyroxene and orthopyroxene – 20%, biotite – up to 1%, quartz – 2-3%, ore minerals – 3- 4%, carbonate, potassium feldspar, apatite Leucocratic, silicified, slightly biotitized gabbro. Composition: plagioclase – 65-70%, 6. 2.6 m orthopyroxene – 12%, quartz – 8-10%, apatite – 6-8%, ore minerals – 2-3%, biotite Pyroxene, biotite-pyroxene, grey to dark-grey, granitized mafic gneiss with development of 7. coarse-grained pyroxene-plagioclase rock with plagioclase content 70-75%. In places 5.6 m enriched with dark-color minerals plagioclase content – 15-20%, pyroxene predominates Biotite-pyroxene enderbite with two-pyroxene, dark-grey, fine-grained mafic gneiss xenoliths 8. 8.5 m up to 0.8 m thick Two-pyroxene, grey, medium-grained, extensively silicified, granitized mafic gneiss, in 9. 25.3 m places up to leucocratic enderbite, somewhere enderbite-pegmatite is noted Medium-coarse-grained, irregularly-grained, in places leucocratic pegmatoid enderbite with 10. 0.1-0.5 m thick xenoliths (up to 10% by volume) of amphibole-two-pyroxene, biotite-two- 26.8 m pyroxene mafic gneiss (pyroxene – up to 35%, biotite – up to 20%) Biotite-two-pyroxene, grey, light-grey, fine-grained, extensively granitized mafic gneiss with 33.5 m 11. pegmatoid enderbite enclaves. At the end of run – fine-medium-grained biotitized gabbro 2.1 m Alternating bands of pegmatoid enderbite and pyroxene mafic gneiss with single quartz 12. 14.0 m grains 13. Leucocratic biotite enderbite 2.5 m 14. Biotite-pyroxene medium-coarse-grained enderbite 2.0 m 15. Pyroxene, amphibolized, biotitized mafic gneiss 0.4 m 16. Leucocratic, coarse-medium-grained, pyroxene-biotite-bearing enderbite 6.4 m 17. Biotite-pyroxene enderbite-migmatite 2.9 m 18. Pyroxene-biotite enderbite-pegmatite 2.8 m 19. Biotite-pyroxene, banded enderbite-migmatite (opaque minerals – 5-7%) 4.7 m 20. Medium-fine-grained silicified enderbite 3.5 m 21. Enderbite-pegmatite 0.8 m Pyroxene, extensively silicified, granitized mafic gneiss. Contains inter-layer bodies of 22. 16.4 m gabbro-norite and norite 0.1-0.5 m thick Two-pyroxene, greenish-grey, in places silicified mafic gneiss. Composition: plagioclase – 40-50%, clinopyroxene – 30-35%, orthopyroxene – 20-25%, biotite – single grains, ore 23. 1.5 m minerals – 1-2%, quartz – single grains; in places rock is enriched in pyroxene and over there hornblende – up to 2-3%, biotite – up to 3% are observed Biotite-two-pyroxene, grey, dark-grey, fine-grained to medium-fine-grained, in places granitized mafic gneiss. Composition: plagioclase – 55%, quartz – from 0 to 10-20% at 24. 9.2 m granitization points, orthopyroxene – 12-15%, clinopyroxene – up to 3%, biotite – 7-10%, ore minerals - up to 3%, apatite – single grains Alternating coarse-grained, in places pegmatoid enderbite, and pyroxene mafic gneiss up to 25. 0.2 m thick. Mafic gneiss composition: pyroxene: rhombic - about 40%, monoclinic – single 3.3 m grains, plagioclase – up to 55%, ore minerals – 5%, K-feldspar (in plagioclase) – 3-4% Pyroxene-biotite enderbite, at the bottom with garnet, rare xenoliths (up to 15 cm thick) of 26. 4.1 m pyroxene-biotite mafic gneiss Pyroxene, grey, dark-grey, regularly-fine-grained, massive mafic gneiss. Composition: plagioclase – 50%, clinopyroxene – 25%, orthopyroxene – 20%, ore minerals – 5%, biotite 27. 1.2 m and apatite – single grains. In places orthopyroxene – up to 43%, clinopyroxene – 1-2%, plagioclase – 50-55%, ore minerals – 3%, quartz, biotite – single grains 28. Garnet-biotite pegmatoid granite 0.9 m 29. Biotite-garnet plagiogranite 2.0 m 30. Leucocratic enderbite 1.2 m 31. Biotite plagiogranite 1.7 m 32. Garnet-biotite-pyroxene enderbite 6.4 m Total thickness 252.7 m

The major distinction of the Sequence column in Verbkivska site is occurrence of carbonate rocks – marbles and calciphyres. Over there DH 1801 has intersected from bottom to top:

Pyroxene, biotite-pyroxene enderbite with xenoliths of biotite-two-pyroxene mafic gneiss 1. 34.5 m from 3-5 to 50 cm thick 2. Biotite pegmatoid granite 5.5 m Pyroxene enderbite with biotite, cataclased, with rare xenoliths up to 0.5 m thick of 3. 33.4 m extensively altered biotite-pyroxene-amphibole mafic rock 4. Leucocratic plagiogranite 5.8 m Two-pyroxene, irregularly granitized (charnockitized) mafic gneiss, with bands of leucocratic and melanocratic composition. Composition of leucocratic varieties: potassium feldspar- 5. perthite – 65%, orthopyroxene – 25%, quartz – 5%, serpentine, apatite, magnetite. 39.8 m Composition of melanocratic varieties: pyroxene – 40-45%, plagioclase and quartz – by 20- 25%, sericite, magnetite – up to 3%, apatite Pyroxene, medium-grained, massive calciphyre. Pyroxene (up to 25%) is dark-green, almost 6. 0.2 m black and light-green 7. Orthopyroxene, low-quartz (up to 5%) enderbite 7.8 m Magnesium, light-grey, fine-medium-grained, massive skarnoid. Composition: diopside – 8. 0.2 m 75%, plagioclase replaced by scapolite – 10%, carbonate – 15%, sphene Pyroxene, melanocratic enderbite. Composition: plagioclase-antiperthite – 60%, 9. 5.8 m orthopyroxene – 20%, quartz – 3%, biotite – 3%, carbonate, apatite Carbonate-pyroxene, light-grey, fine-medium-grained skarnoid. Composition: clinopyroxene 10. 1.8 m – 70%, carbonate – 30%, plagioclase – single grains almost completely replaced by scapolite Pyroxene, grey, fine-medium-grained, irregularly-grained, silicified mafic gneiss. 11. Orthopyroxene is replaced by amphibole, mica, serpentine, carbonate. Secondary quartz – 10- 4.1 m 15% Dolomite-calcite marble with pyroxene (from 2-5 to 30% in some bands), white, medium- 12. grained, massive. Composition: carbonates – 80% (dolomite is replaced by calcite), 0.3 m serpentinized clinopyroxene – 20% in average, antigorite, chrysotile Pyroxene enderbite, mainly leucocratic, with scarce xenoliths of altered mafic gneiss; the 13. 45.0 m rocks are cataclased Two-pyroxene, grey, pink-grey, medium-grained, often irregularly-grained, cataclased, slightly K-feldspatized mafic gneiss. Composition: plagioclase – 70-80%, hypersthene – 10- 14. 25%, clinopyroxene – single grains, ore minerals – 1-2%, apatite – up to 5%, zircon, 6.5 m sulphides. Secondary minerals, epidote, serpentine, sericite, muscovite, potassium feldspar, quartz – up to 5%, carbonate 15. Leucocratic, biotite-pyroxene-bearing enderbite 3.0 m Fine-medium-grained, cataclased enderbite with irregularly distributed pyroxene (from 5-10 16. 7.0 m to 20-30%), in places biotitized (up to 10% of biotite) Pyroxene, pink-grey to grey, fine-medium-grained to coarse-grained, irregularly K- 17. feldspatized mafic gneiss, with quartz content 1-3%, at the top cataclased, extensively 31.5 m biotitized Total thickness 235.0 m

In DH 1802 the contact is intersected between the sequence described above and syenites of Proskurivskiy complex. Over there mafic gneisses and carbonate rocks underwent extensive metasomatic alteration. The fragment of Tyvrivska sequence column is as follows over there (from bottom to top):

Biotite-amphibole-pyroxene, metasomatically altered gneiss. Composition: plagioclase – 1. 75%, microcline – up to 5%, clinopyroxene – 15% (after pyroxene – amphibole, biotite, 1.0 m distinct isometric carbonate grains), sphene, apatite Light-grey to white, fine-medium-grained, massive calciphyre with pyroxene gneiss bands. 2. Composition: carbonate – 65-70%, clinopyroxene – 10-15%, potassium feldspar – 10-15%, 1.8 m plagioclase – 5-10%, sphene, garnet, apatite, ore minerals, serpentine, quartz

18 Thin intercalation of carbonate rock and pyroxene, pyroxene-biotite, biotite gneiss. Band 3. 3.4 m thickness – from 0.5-2.0 to 10.0 cm Light-grey to white, medium- to coarse-grained, massive calciphyre. Composition: carbonate 4. 4.2 m – 80%, pyroxene – 15%, feldspars 5. Syenite with minor altered xenoliths of pyroxene gneiss 31.1 m Marble with chondrodite, in places carbonate-feldspar amphibole-mica metasomatite. 6. 8.5 m Composition: calcite – 85%, chondrodite – 10%, muscovite, colorless amphibole (tremolite?) 7. Mica-feldspar metasomatite with relict pyroxene grains, apatite 2.8 m White, medium-grained, massive marble. Composition: calcite – 90%, tremolite – 4-5%, 8. 15.1 m pyroxene completely replaced by serpentine, quartz (single grains), magnetite 9. Quartz-feldspar metasomatite 2.1 m 10. White calciphyre, medium-grained, massive, contains altered pyroxene, mica, quartz, sphene 1.5 m Total thickness 71.5 m

In Litynskiy dome, besides pyroxene mafic gneisses and gneisses, the leucocratic granulites are widespread, intersected by drill-holes of deep geochemistry and most studied by the interpretation DH 8 in adjacent territory [23]. These are quartz-feldspar rocks with opaque minerals content up to 1%, alternating with biotite-pyroxene gneisses with increased magnetite content. The column of Tyvrivska sequence at Kovalenkivska site is identical to the column of Verbkivska site but amount of carbonate rocks is much less. Two-pyroxene mafic gneisses, biotite-pyroxene, biotite-amphibole-pyroxene, pyroxene-amphibole mafic gneisses and gneisses, amphibolites. Mafic gneisses predominate in Tyvrivska sequence. These include pyroxene, mainly plagioclase rocks with quartz content 5-8, rarely up to 10%. In xenoliths within diverse granitoids they are observed in the outcrops along South Boug, Zgar rivers, as well as in the prospecting and mapping drill-holes. Visually these are grey, dark-grey, greenish-grey, fine- to medium-grained, massive, rarely banded rocks. Under microscope texture is grano-, heteroblastic, in places pseudo-diablastic with elements of poikiloblastic. Mineral composition of fresh rocks in average: plagioclase – from 30 to 60-65% (rarely 40-55%), hypersthene – 10-30% (in essentially orthopyroxene varieties about 20-30%), diopside – up to 30%, biotite – up to 15%, quartz – from 2-3 to 7-10%, often absent. Amphibole varieties of mafic gneisses are studied by mapping drill-holes. They contain from 10 to 35% of hornblende, 15-25% of pyroxenes. Accessory and ore minerals: zircon, sphene, apatite, magnetite, ilmenite, sulphides. Plagioclase is mainly andesine-labrador, in granitized varieties – oligoclase-andesine. Ratio of rhombic and monoclinic pyroxenes is quite variable. At the sequence bottom hypersthene predominates. Diopside is characteristic for the places of alternating two-pyroxene mafic gneisses and carbonate rocks. Gneisses of biotite-pyroxene and amphibole-pyroxene are much less developed than mafic gneisses. Macroscopically they differ from mafic gneisses with lighter color and coarser banding. Rock texture under microscope is lepido-granoblastic, in places cataclastic. Plagioclase content – 50-65% (oligoclase-andesine), quartz – 15-25%, potassium feldspar – perthite – 10-20%, pyroxenes – from 5 to 25%, biotite – from 3 to 12% (in places up to 20%), often garnet appears and in places graphite. Accessory and ore minerals: apatite, zircon, ilmenite, rarely magnetite. Secondary minerals in mafic gneisses and gneisses include serpentine, epidote, sericite, carbonates. 3 Two-pyroxene and hornblende-two-pyroxene mafic gneisses are highest in density (σavg. = 3.01 g/cm ) -6 and magnetization (æavg. = 5411×4π×10 CI units). In magnetic field these rocks are expressed in the linear elongated or ring positive anomalies 1000-2000 nTl in amplitude. 3 Hypersthene mafic gneisses and gneisses are also high-density (σavg. = 2.91 g/cm). Magnetic -6 susceptibility and residual magnetization are low (æavg. = 76×4π×10 CI units). These varieties are expressed by the linear-elongated positive local gravity anomalies and negative magnetic field. However, some magnetic varieties of hypersthene mafic gneisses and gneisses are noted (about 3% of samples) and their distribution fields are expressed in magnetic field. Density of biotite-pyroxene, biotite-amphibole-pyroxene gneisses and mafic gneisses is 2.81 g/cm3, magnetic susceptibility – 540×4π×10-6 CI units. In magnetic field these rocks are expressed in magnetic anomalies from 500 to 1000 nTl in amplitude. In the gravity field they correspond to the local maximums δga 0.5-1.0 mGal in magnitude. By petrochemical features mafic gneisses are similar to ultramafic and mafic rocks. They mainly correspond to high-alumina, in some respect high-magnesium tholeiites and calc-alkaline basalts.

19 Gneisses of the Sequence by petrochemical features correspond to the andesite-basalts and andesites [31, 57]. Amphibolites, according to P.F.Bratslavskiy [14], are only developed in the lower part of Tyvrivska sequence. Macroscopically these are dark-grey, dark-greenish-grey to black rocks, fine-grained, with massive structure, in places granitized. Opaque mineral is dark-green amphibole (hornblende), fine-grained, arranged in aggregates up to 2-4 mm in size. Texture of amphibolites is hetero-granoblastic, grano-nematoblastic, nematoblastic. Structure is massive, in places unclear parallel. Rock composition: amphibole (green, brown-green hornblende) – 60-65%, monoclinic pyroxene (diopside) – 20%, plagioclase oligoclase-andesine (No. 34, 35) – up to 30%, quartz – up to 2%, biotite – 1-2%; minor: apatite, magnetite, zircon, sulphides, chlorite, carbonate. Amphibolites are high-density (3.03 g/cm3 in average), with high values of magnetic susceptibility -6 -3 (4682×4π×10 CI units) and residual magnetization (Ir = 1604×10 A/m). The biggest amphibolite body is noted to the east of Litynka village. In magnetic field it is expressed in some positive second-order maximums up to 1000 nTl in amplitude. Garnet-pyroxene-biotite, pyroxene-biotite gneisses, often with garnet, cordierite and sillimanite, in places with graphite. These rocks are mainly developed in the southern part of map sheet. In association with pyroxene mafic gneisses they constitute winding bodies 7-8 km long and 1-3.5 km wide, with various granitization degrees. Macroscopically these are grey, pink-grey, in places with greenish shade, fine-grained rocks with clear banded structure caused by the leucocratic and melanocratic layer intercalation. Normally these are plagiogneisses with plagioclase content 40-45%, quartz – 25-35%, biotite – 5-10% (in places up to 20%), pyroxene – up to 5-7%, garnet – 5-12%, often with graphite up to 3-5%, in places cordierite and sillimanite whose content attains the level of rock-forming minerals. Physical properties of biotite-garnet and biotite-pyroxene-garnet, often graphitized gneisses of Tyvrivska sequence are similar to those of the Bereznynska sequence rocks. They are equally expressed in physical fields and by these reasons their subdivision is highly complicated. By magnetic properties (æavg. = 49×4π×10-6 CI units) they are close to hypersthene mafic gneisses but notably differ from the latter by density 3 (σavg. = 2.83 g/cm ). Normally biotite-garnet gneisses are expressed in positive gravity anomalies 0.7-1.0 mGal in amplitude and gentle negative magnetic field or positive magnetic anomalies up to 200 nTl. Marbles, calciphyres, skarnoids. Carbonate rocks in Tyvrivska sequence are developed in the south of map sheet in association with biotite-two-pyroxene, biotite-amphibole-pyroxene, pyroxene-biotite mafic gneisses, and in the north-east, besides mentioned rocks, also in tight association with biotite, garnet-cordierite- biotite, amphibole- and pyroxene-biotite gneisses. The contacts with host rocks are both gradual and sharp. Calciphyres constitute the batches of thin intercalation. Maximum thickness of calciphyres in the north-east is 3- 3.4 m. Macroscopically calciphyres are light-grey to dark-grey, fine-medium-grained, massive, in places gneiss- like rocks composed of mainly carbonate – calcite (rarely dolomite). Texture is hetero-granoblastic. Mineral composition: carbonate – 60-70%, olivine, serpentine – 7-8%, pyroxene – 13-30% (diopside), amphibole – up to 10%, plagioclase – 1-10%, scapolite – from 10% to 45%, quartz – 1-10%, phlogopite, biotite, apatite, sphene, spinel, ore minerals – single grains. The rock consists of xenoblastic carbonate crystals while all other minerals in various amounts are contained in between. The marbles are calcitic, rarely dolomite-calcite, white, medium-grained, massive. Like calciphyres they constitute the batches if thin intercalation together with mafic gneisses and gneisses; in Verbkivska site maximum marble layer thickness is 15.0 m. The rock texture under microscope is granoblastic, hetero-granoblastic, rarely lepido-granoblastic, in places rimming. Carbonate content is from 75-80 to 100%, clinopyroxenes – up to 20%, amphiboles – 1-5%, mica – up to 10%, quartz – single grains, ore mineral (magnetite) – single grains. Under influence of granitization processes and also at the contacts with intrusive rocks of Proskurivskiy complex the carbonate rocks and high-calcium mafic gneisses undergo skarnation. Skarnoids are most studied in Verbkivska site. They constitute the bodies from 0.2 to 4.0 m thick. Mineral composition is variable depending on the source rocks. Carbonate-pyroxene skarnoids are light-grey, fine-medium-grained rocks of the following composition: carbonate – 55-60%, pyroxene – 25-30%, amphibole – 10-15%, plagioclase – 1-2%, scapolite – first percents. Magnesium varieties comprise light-grey, fine-medium-grained rocks, massive, composed of diopside – up to 75%, plagioclase – 10-15%, carbonate – 10-15%. Skarnoids from DH 1806 are observed within enderbites and two-pyroxene (mainly clinopyroxene) mafic gneisses and apparently was formed after the latter. Carbonates are almost completely lacking. Their composition: diopside – 35-40%, scapolite – 45-55%, sphene – up to 10%.

20 At the contacts with syenites of Proskurivskiy complex essentially potassium feldspar rocks are developed with microcline-perthite – up to 95%, often with relic sodium plagioclase, pyroxene, completely replaced by hornblende, serpentine and carbonates. After the physical property measurements in 10 skarnoid samples are high-density and actually non- 3 -6 -3 magnetic: σavg. = 2.91 (from 2.82 to 3.24) g/cm , æavg. = 29×4π×10 CI units, Ir = 2×10 A/m. -6 Carbonate rocks (calciphyres, marbles) are non-magnetic (æavg. = 15×4π×10 CI units) with average density 2.78 g/cm3. By their physical properties they are close to gneisses and plagiogranites of garnet-biotite composition. On the background of the hosting two-feldspar Berdychivski granites and migmatites they cause positive anomalies δga. According to many authors (V.A.Stadnyk, I.F.Shramenko, E.V.Melnychuk) and based on the rock geochemistry [17] the calciphyres in Tyvrivska sequence can be considered as metasomatic rocks. Leucocratic granulites. These are light-grey, in places with pink shade, fine-grained, massive rocks. Under microscope the rock texture is grano-hyaloblastic, fine-grained. Mineral composition: plagioclase – oligoclase (anti-perthyte) – 45-80%, granulated quartz – 20-30%, potassium feldspar – from 1 to 15-35%, biotite – up to 1%, pyroxene – single grains, zircon, magnetite. According to B.S.Germanov (set of 14 samples), the range of granulite density is from 2.62 to 2.68 g/cm3, magnetic susceptibility – from 490 to 6012×4π×10-6 CI units, residual magnetization – from 85 to 16194×10-3 A/m (being 1647×10-3 A/m in average). Granulites are expressed in the high-gradient second-order magnetic anomalies some thousand nTl in amplitude (on the background of extensive mosaic magnetic field induced by enderbites and mafic gneisses) which coincide with the local gravity anomalies higher than 1.0 mGal. Granulites are most developed in around and inside Litynska dome structure.

Bereznynska sequence (AR1br)

Bereznynska sequence of Dnistersko-Buzka Series, together with the products of its ultra-metamorphic re-working, constitutes the major backbone of the studied area. The Sequence rocks are most developed in the graben-like structures, in the anticline limbs, and in the intra-dome synclines. The Sequence includes high-alumina garnet-biotite and biotite-garnet gneisses, often with cordierite, sillimanite, in places pyroxene, as well as graphite-bearing gneisses. Pyroxene mafic gneisses in the Sequence are observed in the thin interbeds. The Sequence is most developed in the central part of map sheet although large enough bodies are also noted in the northern and north-western parts. Bereznynska sequence rocks are mainly positioned within garnet-biotite two-feldspar granites, rarely plagiogranites of Berdychivskiy complex, somewhere after these rocks charnockitoids of Litynskiy complex are developed. The biggest fields of the Sequence rocks are encountered in the area of Kudymka, Kovalenky, Molochky, Veselka, Maliy Brataliv villages. Minor bodies are observed in the outcrops along Sluch and South Boug rivers. From the individual fragments of Bereznynska sequence, its column looks as follows: the major part is composed of garnet-biotite in places with cordierite gneisses, graphite-biotite and biotite gneisses, and at the column bottom – pyroxene-biotite, biotite-pyroxene, amphibole-pyroxene mafic gneisses and gneisses. The most representative Sequence column fragment is studied by the drill-hole profile nearby Kudymka village. Despite of extensive granitization, superimposed hydrothermal-metasomatic and tectonic changes, all the Sequence rock varieties are developed over there making possible to define some regularities in the Sequence structure. In the profile, the limb of synform structure with dipping to the south-west under the angle 55-60o is drilled out.

1. Garnet-biotite migmatite 1.5 m 2. Leucocratic garnet-cordierite-biotite-bearing granite 0.8 m 3. Garnet-biotite migmatite with cordierite 2.7 m Biotite-pyroxene gneiss, graphite-bearing, greenish-grey, fine-grained, thin-banded, silicified. 4. Composition: plagioclase – 55%, quartz – 20%, hypersthene – 15%, biotite – 8%, graphite – 0.4 m 2%, apatite – 1% 5. Garnet-biotite migmatite (extensively irregularly granitized gneiss) with cordierite, cataclased 1.7 m Graphite-biotite, grey, fine-grained, unclear-banded, silicified, cataclased gneiss. 6. 0.5 m Composition: plagioclase – 50%, quartz – 25%, biotite – 15%, graphite – 8% 7. Leucocratic granite with garnet, scarce cordierite and biotite pods, cataclased 0.5 m

21 Garnet-biotite gneiss with cordierite, grey, medium-fine-grained, highly granitized, 8. 3.1 m cataclased, sulphidized, silicified Leucocratic, garnet-bearing granite with thin (up to 5-10 cm) xenoliths of graphite-biotite 9. 9.4 m gneiss at the top Garnet-graphite-biotite gneiss, grey, fine-medium-grained, spotty, unclear banded under 10. angle 15-25o to the core axis, irregularly granitized. Composition: plagioclase and quartz – 3.8 m 70%, biotite – 18%, graphite – 12% 11. Leucocratic, cordierite-garnet-bearing granite 3.6 m 12. Two-feldspar (plagioclase – 40%, orthoclase – 25%), garnet-biotite granite 6.6 m 13. Leucocratic granite with scarce cordierite, garnet, very rarely biotite pods 2.9 m 14. Garnet-biotite, grey, medium-fine-grained, massive gneiss 3.5 m Leucocratic, coarse-grained to pegmatoid granite, with scarce cordierite pods and single 15. 4.1 m garnet and biotite grains Garnet-biotite, grey, diverse-grained, mainly medium-grained, extensively granitized gneiss. 16. 5.9 m Composition: plagioclase and quartz – 70%, orthoclase – 10%, garnet – 12%, biotite – 10% Leucocratic, biotite-bearing granite, often with cordierite. Alternates with cordierite-biotite, graphite-biotite with cordierite migmatite. Xenolith 0.3 m thick of granitized biotite- 17. 9.7 m pyroxene, greenish-grey, fine-grained gneiss with unclear banding under the angle 30-55o to the core axis Biotite-graphite gneiss, somewhere pyroxene-bearing, fine-grained, silicified, chloritized, 18. 2.2 m pyritized. Composition: plagioclase – 60%, quartz – 20%, biotite – 8%, graphite – 12% 19. Leucocratic, biotite-cordierite-bearing granite 2.0 m Biotite-graphite gneiss with scarce cordierite and garnet grains, granitized in various extents, 20. 3.3 m silicified, sulphidized Leucocratic, biotite-cordierite-bearing granite, at the top with thin (5-10 cm) scarce xenoliths 21. 4.1 m of graphite-biotite, extensively granitized gneiss with sulphide mineralization (2-3%) Leucocratic, orthoclase-perthite granite, in places enriched in cordierite and biotite, rarely biotite and graphite. Alternates with skialites and xenoliths (up to 30 cm thick) of biotite 22. gneiss with graphite, rarely pyroxene. Two xenoliths (0.5 and 0.9 m thick) of biotite-two- 14.4 m pyroxene, greenish-grey, fine-grained mafic gneisses at the bottom. Composition: plagioclase – 60%, orthopyroxene – 32%, clinopyroxene – 6%, quartz – 10%, sulphides – 2-3% Alternating leucocratic garnet-bearing granite and graphite-biotite gneiss, grey, fine-grained, thin-banded, variously-granitized, sulphidized. Composition: plagioclase – 35%, quartz – 23. 13.0 m 30%, biotite – 15%, graphite – 20%, chlorite, pyrite. At the bottom – 0.3 m thick graphite- biotite gneiss with pyroxene 24. Biotite migmatite with cordierite, in places with garnet 6.0 m Biotite-two-pyroxene mafic gneiss, banded under the angle 15-20o to the core axis, silicified, 25. 0.7 m sulphidized 26. Leucocratic orthoclase-perthite granite with scarce garnet, biotite, cordierite grains 8.6 m Graphite-biotite gneiss with pyroxene, greenish-grey, fine-grained, thin-banded, silicified, 27. albitized. Composition: plagioclase and quartz – 80%, biotite – 4%, graphite – 2%, 3.7 m orthopyroxene – 3%, albite – 10% Alternating leucocratic biotite-cordierite-bearing granite and graphite-biotite gneiss, grey to 28. 11.5 m greenish-grey, fine-grained, silicified, chloritized, sulphidized Garnet-cordierite-biotite migmatite with 5-30 cm thick “interbeds” of pyroxene, fine-grained, 29. thin-banded, amphibolized, silicified gneiss. Composition: plagioclase – 50%, quartz – up to 7.3 m 20%, hypersthene – 16%, biotite – 11%, graphite, pyrite – 2-3%, amphibole, scapolite 30. Leucocratic, orthoclase-perthite, biotite-cordierite-bearing granite 3.2 m Alternating biotite cordierite-bearing granite and graphite-biotite migmatite. The rocks are cataclased. In the mid – thin xenoliths of graphite-biotite, greenish-grey, sheared, silicified, 31. 14.0 m sulphidized gneiss. Composition: plagioclase and quartz – 90%, biotite – 5%, graphite – 3%, apatite, pyrite – 2% Alternating cordierite-graphite-biotite migmatite, leucocratic granite and predominating 32. biotite-graphite, grey, diverse-grained, granitized gneiss. Composition: plagioclase – 60%, 22.0 m orthoclase – 10%, quartz – 20%, graphite – 5%, biotite – 3% Leucocratic granite with scarce garnet, biotite, cordierite pods. Relicts of biotite-cordierite 33. 8.0 m granitized gneiss

22 Alternating leucocratic granite and graphite-biotite, chloritized, pyritized gneiss. Gneiss 34. composition: plagioclase – 40%, potassium feldspar and quartz – by 20%, biotite – 14%, 22.0 m graphite – 7%, chlorite, pyrite Alternating pegmatoid granite and graphite-biotite irregularly granitized gneiss. Thickness of 35. gneiss layers – 20-30 cm. Gneiss composition: plagioclase – 40%, quartz – 20%, graphite – 22.6 m up to 12%, biotite – 9%, chlorite, pyrite Biotite-two-pyroxene, greenish-grey, fine-grained, granitized, sheared mafic gneiss. 36. Composition: plagioclase – 40%, orthopyroxene – 10%, clinopyroxene – 30%, quartz – 10%, 0.6 m biotite – 9% Graphite-biotite, grey, fine-grained, granitized, cataclased, sulphidized gneiss. Composition: 37. 2.0 m plagioclase – 55%, quartz – 25%, biotite – 11%, graphite – 10%, pyrite 38. Leucocratic biotite-garnet-bearing granite 3.8 m Biotite-two-pyroxene, grey, fine-grained, granitized mafic gneiss, unclear-banded under the 39. angle 20o to the core axis, at the contacts – cataclased. Composition: plagioclase – 40%, 3.5 m clinopyroxene – 32%, orthopyroxene – 5%, quartz – 18%, biotite – 4% Garnet-graphite-biotite, grey, fine-grained, granitized, cataclased, sulphidized gneiss. 40. Composition: plagioclase – 40%, quartz – 20%, biotite – 21%, garnet – 10%, graphite – 9%, 0.8 m sulphides Garnet-biotite, biotite granite, with minor xenoliths of granitized granite-biotite gneiss. 41. Gneiss composition: plagioclase – 40%, quartz – 20%, biotite – 12%, graphite – 7%, 10.7 m potassium feldspar – 20% Alternating garnet-biotite migmatite, biotite granite with scarce cordierite grains, and 42. 15.5 m pegmatoid granite 43. Garnet-biotite, graphite-bearing, pink-grey, fine-grained, massive gneiss 5.5 m

In view of confident enough correlation of the columns, supported by the electric correlation studies (hole-to-hole version), the Sequence column is added up by the following rocks:

Graphite-biotite, fine-grained gneiss, banded under the angle 40-50o to the core axis, highly 1. granitized, sheared, sulphidized. Composition: plagioclase – 50%, quartz – 25%, biotite – 5.6 m 14%, graphite – 11%, pyrrhotite, pyrite Alternating graphite-biotite, chloritized, sulphidized gneiss and leucocratic granite. Gneiss 2. composition: plagioclase – 50%, quartz – 25%, biotite – 11%, graphite – 9%, chlorite, pyrite, 10.3 m pyrrhotite, chalcopyrite, molybdenite 3. Leucocratic orthoclase-perthite granite 1.0 m Graphite-biotite gneiss with scarce garnet grains, grey, fine-medium-grained, highly 4. granitized, sulphidized, sheared. Composition: plagioclase – 50%, quartz – up to 30%, biotite 3.3 m – 13%, graphite – 7%, cordierite, sulphides 5. Leucocratic granite 0.5 m Graphite-biotite gneiss with garnet, granitized, pyritized, sheared. Composition: plagioclase – 6. 9.1 m 55%, quartz – 25%, biotite – 8%, graphite, garnet – 4%, apatite – 1%, pyrite 7. Leucocratic orthoclase-perthite granite 2.4 m Biotite-graphite, unclear-banded, variously-granitized, sheared, sulphidized gneiss. 8. 2.6 m Composition: plagioclase – 56%, quartz – 26%, graphite – 11%, biotite – 7%, pyrite 9. Graphite-biotite gneiss, extensively silicified, albitized, sulphidized 5.4 m 10. Leucocratic, orthoclase-perthite, biotite-bearing granite 4.4 m 11. Melanocratic biotite migmatite 2.1 m Graphite-biotite, fine-grained, massive, sheared, in places milonitized, silicified, chloritized 12. gneiss. Composition: plagioclase – 30%, quartz – 20-30%, biotite – 20%, graphite – 20%, 1.0 m chlorite 13. Leucocratic biotite granite 6.9 m 14. Leucocratic biotite-bearing granite, to the bottom – tectonite after granite 6.0 m 15. Tectonite after granite 10.0 m Alternating pyroxene-biotite migmatite, biotite-two-pyroxene mafic gneiss, graphite-biotite gneiss and leucocratic granite. Mafic gneiss composition: hypersthene – 29%, clinopyroxene 16. 12.6 m – 12%, plagioclase – 42%, quartz – 11%, biotite – 6%, pyrite. Gneiss composition: plagioclase and quartz – 60%, biotite – 17%, graphite – 12%, apatite, pyrite

23 17. Biotite migmatite 16.6 m 18. Leucocratic orthoclase-perthite granite 3.9 m Biotite-two-pyroxene, dark-grey with greenish shade, fine-grained, massive, sheared mafic 19. gneiss. Composition: plagioclase and quartz – 42%, orthopyroxene – 30%, clinopyroxene – 0.6 m 23%, biotite – 5% Alternating leucocratic granite and biotite gneiss with graphite. Thickness of gneiss 20. “interbeds” from 0.4-0.7 to 2.4 m. In some places biotite and graphite are contained in equal 17.9 m amounts – up to 8% Graphite-garnet-biotite, graphite-biotite, in places biotite-graphite, sheared, sulphidized 21. gneiss. Composition: plagioclase – 50%, quartz – 25%, biotite – 8%, garnet – 5%, graphite – 6.3 m 3% (in garnet-less varieties up to 9-10%), chlorite, pyrite 22. Leucocratic granite with scarce up to 0.5 m thick xenoliths of graphite-biotite gneiss 24.3 m 23. Orthoclase-perthite, biotite-bearing, silicified, sulphidized granite 7.0 m Biotite-two-pyroxene, dark-grey, medium-fine-grained, in various extents granitized mafic gneiss. Composition: plagioclase – 47%, orthopyroxene – 14%, clinopyroxene – 28%, quartz 24. 6.3 m – 5%, biotite – 5%. In the higher granitized varieties pyroxenes content decreases to 10-25% and biotite and quartz increases up to 15-25% Biotite-graphite, dark-grey, fine-micro-grained gneiss, thin-unclear-banded under the angle 25. 45o to the core axis, at the top granitized. Composition: plagioclase – 55%, quartz – 21%, 3.8 m graphite – 15%, biotite – 9% Leucocratic, medium-coarse-grained to pegmatoid granite with xenoliths of graphite-biotite 26. 6.1 m gneiss from 3-5 to 10-15 cm thick Graphite-biotite, dark-grey gneiss, thin-banded under the angle 45-50o to the core axis, 27. granitized. Composition: plagioclase – 53%, quartz – 26%, biotite and chlorite – 14%, 1.1 m graphite – 7%, apatite Leucocratic orthoclase-perthite granite with scarce biotite flakes and single garnet grains, 28. 6.1 m cataclased Graphite-biotite-garnet, dark-grey, fine-grained gneiss, banded under the angle 35-50o to the 29. core axis, with scarce thin (5-20 cm) interbeds of pegmatoid granite. Composition: 6.8 m plagioclase – 40%, quartz – 30%, garnet – 16%, biotite – 8%, graphite – 5%, zircon, apatite Garnet-biotite plagiogranite with numerous xenoliths 5-15 cm thick (rarely up to 1 m) of 30. 16.3 m garnet-biotite gneiss Graphite-hypersthene-biotite-garnet, dark-grey, fine-grained, massive gneiss. Composition: 31. plagioclase – 50%, quartz – 24%, garnet – 10%, biotite – 7%, hypersthene – 6%, graphite – 5.9 m 10% Pegmatoid orthoclase-perthite granite. At the top (2.0 m thick) and bottom (1.5 m) xenoliths 32. 31.6 m of garnet-biotite gneiss Graphite-biotite-garnet, grey to dark-grey, fine-grained, massive gneiss. Composition: 33. 5.8 m plagioclase – 60-65%, quartz – 15-20%, garnet – 15-20%, biotite – up to 5%, graphite – 50% Total thickness 520 m

The central part of synform structure, adding up the column described above, is composed of garnet- biotite, extensively granitized gneisses. Based on the data from geological mapping in the scale 1:50 000 [51], the authors have concluded that biotite-garnet gneisses and plagiogneisses, often with graphite and cordierite, are most developed in Bereznynska sequence. Less developed are graphite-biotite gneisses and mafic gneisses while biotite-hypersthene mafic gneisses occupy the least volume and constitute thin (up to first meters) interbeds. The contact between Bereznynska and Tyvrivska sequences is not identified. In our mind, this mention matches available data in the most extent. Generalized column of Bereznynska sequence, compiled by P.F.Bratslavskiy [15] using fragmented columns of boreholes drilled nearby Veselka village, is 779.3 m of total thickness. However, in the compilation the batches of alternating pyroxene-amphibole, amphibole-biotite gneisses and mafic gneisses with calciphyres were included to the Sequence, although these units are not characteristic for the column of Bereznynska sequence and they probably should be considered as the retrograded rocks of Tyvrivska sequence. In addition, based on the mentioned compilation it was concluded on the gradual contact between Berenynska and Tyvrivska sequences, which, in our mind, is not properly substantiated.

24 The biggest bodies of Bereznynska sequence are mapped close to the Stara Synyava, Podolyany, Veselka villages. Being up to 8.5 km in size, they are irregularly-shaped and elongated in the north-western or sub-latitudinal directions. In Veselkivska graben-like structure Bereznynski rocks constitute the body 2.5 km wide and, according to P.F.Bratslavskiy [15], are flat-laying (20-40o). As noted above, the rocks of Bereznynska sequence are mainly granitized by the two-feldspar and plagiogranitoids of Berdychivskiy complex; the rocks re-working by charnockites of Litynskiy complex is noted. Biotite, garnet-biotite, cordierite-garnet-biotite, in places with sillimanite gneisses. Garnet-biotite gneisses are most developed in Bereznynska sequence. They are observed in the separated, in places large enough (first tens of square kilometers) bodies in the central and north-eastern parts of the area, and also in the external zones of Litynskiy and Medzhybizkiy domes in the south. Almost everywhere the gneisses are granitized in various extents, their transitions into migmatites and granites are gradual, in places the contacts are highlighted by biotite accumulations on the background of the rock grain size increasing. Macroscopically the garnet-biotite gneisses are grey, dark-grey, in places pink-grey, fine-grained, banded, somewhere thin-banded or massive rocks. Under microscope texture is lepido-granoblastic, rarely granoblastic or porphyryblastic, cataclastic with elements of poikiloblastic antiperthite, myrmekite. Structure is parallel, rarely massive. Mineral composition: plagioclase (oligoclase, andesine) – 35-60%, potassium feldspar (orthoclase, rarely microcline) – 5-15%, quartz – 20-30% (this is the highest content for the metamorphic rocks of the Sequence). Amount of opaque minerals (garnet and biotite) varies quite widely, in places attaining 15-20% under the average content of biotite – 5-10%, and garnet – 2-8%. Often cordierite and graphite are observed. Accessories: apatite, zircon; ore minerals: graphite, sulphides; secondary: chlorite, sericite, muscovite, carbonate. Plagioclase in granitized varieties contains antiperthite microcline ingrowths. Garnet is observed in the isometric porhyryblastic aggregates with poikilitic inclusions of quartz grains, plagioclase, biotite flakes, and is also noted in isometric grains 3-5 mm in size. Cordierite-garnet-biotite, in places with sillimanite gneisses are also distributed widely enough. They often alternate with garnet-biotite gneisses occurring in the layers from 2.5 to 27.9 m thick. Visually these are grey, in places light-greenish-grey, fine-medium-grained, banded rocks. Under granitization they are replaced by migmatites with the same composition of opaque minerals. Under microscope rock texture is porphyryblastic, lepido-granoblastic, hetero-granoblastic, poikiloblastic, in places cataclastic; structure is parallel. Mineral composition: plagioclase – 40-65%, microcline – 5-10%, quartz – 18-35%, biotite – 5-20%, garnet – 5-8%, cordierite – 3-10%, sillimanite – up to 2%; accessories: apatite, zircon, kyanite – up to 1-2%; ore minerals: graphite, sulphides; secondary: carbonate, chlorite, sericite, muscovite. Cordierite is noted both in separate chains and individual enriched bands in gneisses. It is mainly developed in the granitized rocks. Somewhere cordierite is replaced by serpophite and gets light-green shade. Sillimanite is observed in thin-fibrous aggregates of fibrolite. In places it is replaced by mica minerals. Kyanite is only known in the sillimanite-bearing gneiss varieties. Besides the garnet-bearing varieties, high-alumina gneisses also include garnet-less cordierite-biotite, sillimanite-cordierite-biotite, somewhere sillimanite-biotite rocks. They are mainly developed in the upper part of Bereznynska sequence. 3 Garnet-biotite gneisses are of moderate density σavg. = 2.68 g/cm and magnetic susceptibility æavg. = 228×4π×10-6 CI units. Normally garnet-biotite gneisses, occurring in Berdychivski granitoids, are associated with the positive gravity anomalies 0.3-0.7 mGal in amplitude and gentle negative magnetic field or positive magnetic anomalies up to 200 nTl in amplitude. Graphite-biotite, biotite-graphite, biotite gneisses. These rock varieties are mainly developed in the upper part of Bereznynska sequence alternating with the batches of garnet-biotite gneisses. Macroscopically graphite-biotite gneisses are grey and dark-grey (up to almost black), fine-micro- grained, thin-banded rocks. Under microscope texture is lepido-granoblastic, often cataclastic, structure is parallel. Mineral composition: plagioclase (mainly oligoclase) – 50-55%, rarely – 60%, quartz – 20-22%, potassium feldspar (orthoclase) – 10-20%, often lacking, biotite – 3-15%, graphite – from 2 to 10%, in places – up to 15-20%. Accessories: apatite and zircon. Secondary: chlorite, sulphides. Processes of silicification, sulphidization, cataclasm and milonitization are extensively developed. Graphite is observed in the elongated tables, flakes, and is associated with biotite. At the sites of cataclasm and silicification, likewise granitization ones, the coarser graphite flakes are observed. In these cases sulphides, mainly pyrite, are extensively developed. Carbon content attains 3.5-6% [14]. Petrochemical parameters of these varieties are given in the Table 2.1.

25 Physical properties of graphite-biotite gneisses are variable. In 70% of measured samples density value varies in the range 2.60-2.74 g/cm3 (modal value – 2.67 g/cm3), and for 30% – 2.34-2.52 g/cm3. Average density is 2.63 g/cm3, magnetic susceptibility – 46×4π×10-6 CI units (almost non-magnetic varieties). Unequivocal criteria for their distinguishing in the column are polarization anomalies coinciding with the anomalies of increased and high conductivity.

Table 2.1. Petrochemical features of Bereznynska sequence rocks

Biotite gneisses Graphite-biotite gneisses Oxides, ratios X, % Min Max X, % Min Max SiO2 60.9 59.55 62.25 62.66 61.67 63.65 TiO2 0.96 0.9 1.02 0.45 0.39 0.51 Al2O3 16.06 15.88 16.24 13.06 10.96 15.15 Fe2O3 1.47 1.18 1.76 2.98 2.90 3.06 FeO 4.705 4.06 5.35 3.18 2.65 3.71 MnO 0.07 0.05 0.09 0.12 0.10 0.14 MgO 3.52 3.14 3.9 1.27 0.98 1.55 CaO 3.97 3.81 4.12 3.00 2.71 3.28 Na2O 3.35 3.3 3.4 4.08 3.99 4.17 K2O 2.155 2.13 2.18 2.64 2.23 3.04 - H2O ------+ H2O - - - 0.10 0.06 0.13 P2O5 0.09 0.018 0.17 0.06 - 0.11 SO3 0.11 0.1 0.11 3.52 1.47 5.56 Ssf - - - 1.32 0.45 2.19 CO2 ------LOI 2.28 1.7 2.86 1.96 0.98 2.94 Sum 99.88 99.72 100.04 100.37 99.80 100.93 V3 273 198 390 5028 1966 13 600 V4 0.11 0.09 0.15 0.75 0.32 1.76 Na2O+K2O 5.51 5.43 5.58 6.72 6.22 7.21 f 42.5 42 43 58 57 60 F 49 47 50 72 70 75 f0 38 38 38.5 54 49 59

Biotite gneisses are locally developed. They constitute the upper parts of Bereznynska sequence and most often lie over graphite-biotite gneisses, in places over their pyroxene-bearing varieties (with orthopyroxene). Petrochemical parameters are given in Table 2.1. These gneiss varieties by physical properties essentially differ from the garnet-biotite ones. They are less dense and, besides that, some of these rocks exhibit increased magnetic susceptibility: histogram is bimodal -6 (æavg. = 31 and 1029×4π×10 CI units). In Veselkivska structure these rocks are expressed in the linear (north- west-trending) negative anomalies from 0.5 to 1.25 mGal, as well as in the elongated in the same direction magnetic anomalies 100-200 nTl in amplitude. Two-pyroxene, biotite-pyroxene, pyroxene-biotite gneisses and mafic gneisses are developed widely enough but normally occur in thin (0.4-0.7 m, rarely up to 3.5 m) interbeds within garnet-biotite, cordierite- garnet-biotite gneisses in the lower part of Bereznynska sequence. Rarely these rocks are noted in association with graphite-biotite pyroxene-bearing gneisses in the upper column part. And also they are observed in xenoliths in garnet-biotite granites and migmatites. Macroscopically these are grey, dark-grey, greenish-grey, massive, unclear-banded rocks. Under microscope: texture is hetero-granoblastic, nemato-granoblastic, cataclastic. Mineral composition: plagioclase (oligoclase, rarely andesine) – 40-47%, in places orthoclase, quartz – 5-20%, somewhere up to 40%, pyroxene – 5-40%, biotite – 5-10%, amphibole developed after pyroxene (up to formation of pyroxene-amphibole-biotite gneisses); accessories: apatite – up to 2%, zircon, sphene, garnet, tourmaline; ore minerals: sulphides, graphites, magnetite; secondary: muscovite, carbonate, chlorite, epidote (up to 4%), scapolite. The ratio between rhombic and monoclinic pyroxenes is variable. Hypersthene is more frequent while clinopyroxene in places is lacking at all. In two-pyroxene mafic gneisses clinopyroxene exceeds rhombic pyroxene with ratio 2-3:1. These are the

26 varieties where content of pyronexes attains 40%, in places 50%, while in the orthopyroxene varieties hypersthene content is 10-15%. Two-pyroxene, biotite-pyroxene, pyroxene-biotite gneisses and mafic gneisses of Bereznynska sequence by magnetic properties and density are similar to the same rocks of Tyvrivska sequence.

Dnistersko-Buzka Series undivided (AR1db)

These rocks are mapped in the western part of studied map sheet. The rocks are developed at the depth beneath Vendian sediments and are only studied by some mapping boreholes drilled into the basement by 1-5 m, thus, information on the column is limited. The rocks are noted mainly in the southern part of Starokostyantynivskiy enderbite-charnockite dome within both charnockitoids and Berdychivski granites and migmatites. By the geochemical specialization of most widespread rock types in Dnistersko-Buzka Series, using their background-normalized average chemical element values in major rock types [18], the rocks of Tyvrivska sequence (mainly pyroxene-bearing mafic gneisses) display positive chalco-litho-siderophile specialization expressed in the increased contents of molybdenum, nickel, cobalt and copper, removal zone elements: cesium, yttrium, strontium and niobium. While in the west Kc of molybdenum varies from 2.1 to 3.1, then in the east it varies in the range 3.0-3.3; nickel – 1.8-3.1 and 0.4 in the west and east respectively. From this range the calciphyres drop out displaying very strong positive geochemical specialization for niobium, barium, zirconium, cobalt, tin, lanthanum, and negative for lithium, apparently reflecting influence of metasomatic processes on the development of given rock type. Bereznynska sequence, which includes various gneisses with subordinate mafic gneisses, exhibits positive chalco-sidero-lithophyle specialization, also slightly variable in space: in the south – positive for molybdenum, silver, copper, nickel, cobalt, and negative – for germanium, yttrium, niobium; and in the north – positive for molybdenum, copper, lead and deficit in yttrium, beryllium, scandium, lithium, niobium. It should be noted that graphite and graphite-bearing varieties exhibit the highest concentration coefficients of molybdenum, silver, copper and nickel.

21Proterozoic Eonotheme

Proterozoic units include supra-crustal Paleo-Proterozoic rocks, developed in the basement in the map sheet part which belongs to Volynskiy mega-block, and non-metamorphosed volcanogenic-sedimentary rocks of the lower part of sedimentary cover, developed on the slope of Ukrainian Shield and distinguished in Neo- Proterozoic Vendian System.

55Paleo-Proterozoic Eratheme

Novograd-Volynska LTZ

Teterivska Series

Vasylivska Suite (PR1vs(?))

Vasylivska Suite conventionally includes supra-crustal rocks developed in the far north-north-western part of the territory. The fields of their distribution are located to the north-west from the marginal sutures of Teterivska fault zone, and in Andrushivska fault zone from the south are bounded by the sub-latitudinal breaks. In the studied area, likewise Vasylivska Suite stratotype [30], the Suite combines two rock associations: aluminous gneisses and amphibole-bearing rocks (amphibole-biotite, biotite-amphibole gneisses and mafic gneisses and amphibolites). While the first association is characteristic for Bereznynska sequence of Dnistersko- Buzka Series, the second one is not encountered in this sequence. In addition, in Bereznynska sequence aluminous gneisses permanently associate with hypersthene-bearing mafic gneisses and gneisses, whereas in Vasylivska Suite these rocks are not known. Most frequently Vasylivska Suite rocks are developed within amphibole-bearing plagiogranites and granodiorites, typical for Sheremetivskiy complex; the rocks are connected by gradual transitions, similarity in mineral composition, petrochemical and geochemical features, that is, these rocks comprise substratum for ultra- metamorphic development of mentioned granitoids. In contrast, these rock varieties are not characteristic for ultra-metamorphic granites of Berdychivskiy complex developed after the rocks of Dnistersko-Buzka Series.

27 By mineral assemblages the metamorphic degree of Vasylivska Suite does correspond to the amphibolite facies. Granulite assemblages, characteristic for Dnistersko-Buzka Series, are not identified. Evidences for retrograde modifications of granulite rocks under amphibolite facies conditions are not found in the Suite rocks. Thus, to distinguish Vasylivska Suite in the map sheet M-35-XXII the following reasons are taken into account: 1. Occurrence of rock associations characteristic for Vasylivska Suite in the stratotype column. 2. Granitization with development of rocks which most likely belong to Sheremetivskiy complex. 3. Tectonic position at the border between Podilskiy block of Dnistersko-Buzkiy mega-block and Volynskiy mega-block. 4. Metamorphism under amphibolite facies conditions, which is more typical for the rocks of Volynskiy mega-block but not for Podilskiy block. 5. The indirect evidence may comprise intrusion of the Suite rocks by the Bukynskiy complex characteristic for Volynskiy mega-block. In the studied map sheet the Suite in only intersected by single mapping drill-holes in the area of Kipchyntsi – Borushkivtsi – Velyki Derevychi villages, and by these reasons recovery of its column is not possible. By the analogue with the stratotype it can be assumed that in the lower column part the high-alumina gneisses are developed which most authors consider to be the products of re-deposition and metamorphism of weathering crust rocks. The Suite column is added up with the batch of amphibole-bearing rocks, which by chemistry are close to mafic and intermediate meta-volcanics. This column type, with terrigenous facies replacement by volcanogenic facies, may suggest for their development under conditions of intra-continental rift. Apparently, Vasylivska Suite unconformably lies over the rocks of Dnistersko-Buzka Series and charnockitoids but direct observations in the map sheet are lacking. In the lower column part of Vasylivska Suite the high-alumina garnet-biotite, often cordierite-bearing and in places graphitized, are developed. The gneisses, enriched in graphite (up to 10%), are discontinuous and replaced by strike by graphite- bearing (1-5% graphite) varieties. Graphite content increasing is noted in tectonic zones. The features of garnet-biotite gneisses are as follows: the rock texture under microscope is hetero- lepido-granoblastic; mineral composition: plagioclase (andesine-oligoclase) – 40-60%, quartz – up to 20%, biotite – 15-30%, garnet – up to 10%, normally 5%, graphite – up to 8%, cordierite – 1-5%, sillimanite – 1%; accessories: apatite, zircon; ore minerals: magnetite, sulphides (pyrite). Plagioclase is normally poly-synthetically twinned and observed in the grains of irregular tabular shape. The grain size is up to 1.5 mm. Quartz is observed in the grains or irregular intergrowths and quite irregularly distributed in the rock filling the interstices between other minerals. Extinction is wavy. Grains size is 1-2 mm. Biotite is observed in brown, greenish-brown irregular flakes which fill up the interstices between quartz and plagioclase grains; in places it includes fine grains of ore mineral and zircon. Garnet is developed in isotropic grains 0.2-0.3 cm in size. Graphite is normally observed in the intergrowths with biotite. Amphibolites and amphibole-bearing gneisses are characteristic for the upper part of Vasylivska Suite. Amphibolites under microscope exhibit granoblastic, hetero-nematoblastic texture. The rock texture is massive or parallel. Mineral composition: plagioclase – up to 40%, amphibole – up to 70%, biotite – up to 20%, quartz – up to 5%. Plagioclase, mainly andesine, is often sericitized, with inherited from igneous rocks fine amphibole grains. Plagioclase crystal size is up to 20 mm (in porphyryblasts). Amphibole is comprised of the bright-colored green hornblende, in places with slight brown shade. The amphibole grain edges are irregular. Grain size is up to 1 cm. Biotite is observed in the separate brown flakes developed after amphibole. Biotite grains size is up to 0.3-0.4 cm. Quartz is developed in the single elongated grains in amphibole and also fills up the space between amphibole and plagioclase grains. Accessory minerals of amphibolites: sphene – up to 2%, spinel – up to 2-3%, zircon, calcite. Ore minerals: magnetite, pyrite, pyrrhotite, rutile. Secondary: scapolite, pellite, serpentine, chlorite. Amphibole and amphibole-bearing gneisses visually are dark-grey with greenish shade, schistose, rarely massive rocks. Under microscope the rock texture is lepido-granoblastic, lepido-hetero-granoblastic, granoblastic, in places poikilo-porphyryblastic, cataclastic. Mineral composition: plagioclase (oligoclase- andesine) – 45-55%, quartz – 10-25%, biotite – 10-15%, amphibole (hornblende) – 10-15%, in places microcline

28 – up to 2%, cordierite – 5%; accessories: apatite, sphene, zircon; ore minerals: magnetite, sulphides (pyrite, pyrrhotite), graphite. Plagioclase, mainly oligoclase, is observed in the tabular grains, often poly-synthetically twinned, pellitized. Somewhere fine individual antiperthite microcline ingrowths are noted. Quartz in the isometric grains somewhere contains amphibole, biotite, and apatite crystals. Quartz grain size is 0.5-0.8 m. Amphibole comprises green hornblende, rarely tremolite, observed in colorless fine-tabular and prismatic grains from 0.1 to 0.8 cm in size. Biotite is red-brown with clear pleochroism. It is developed after amphibole and observed in the single flakes and their aggregates. Flake size is 0.2-0.5 cm. Average content of major oxides in garnet-biotite gneisses: SiO2 – 64.88-66.26%, Fe2O3 – 1.54-3.13%, FeO – 2.05-4.16%, TiO2 – 0.37-0.65%, CaO – 2.49-3.62%, MgO – 1.38-2.72%, K2O – 2.42-2.99%, Na2O – 2.46-3.05%, P2O5 – up to 0.16%. Chemical composition of amphibolites: SiO2 – 47.0-52.0%, Fe2O3 – 1.27- 3.26%, FeO – 6.45-10.37%, TiO2 – 0.78-1.87%, CaO – 7.0-7.84%, MgO – 5.7-10.28%, K2O – 2.85-3.5%, Na2O – 0.76-3.4%, P2O5 – 0.3-0.5%. The Suite rocks exhibit the following petrophysical properties. Density of amphibole-bearing gneisses depends on migmatization degree and varies in the range 2.72-2.96 g/cm3, and their magnetic susceptibility varies from 9 to 110×4π×10-6 CI units. Density of amphibolites is up to 3.1 g/cm3, magnetic susceptibility – up to 7000×4π×10-6 CI units. By micro-element content garnet-biotite and graphite-garnet-biotite gneisses of Vasylivska Suite display positive geochemical specialization for molybdenum, lithium, silver, copper, and negative – for chromium, cobalt, nickel, and yttrium. By lithium content the gneisses of Vasylivska Suite differ from the rocks of Dnistersko-Buzka Series where negative specialization for this element is established. It should be noted that positive geochemical specialization for silver and copper is typical for the graphite-bearing gneiss varieties only. Amphibolites of Vasylivska Suite exhibit positive geochemical specialization for nickel, cobalt, chromium, molybdenum, copper, and negative – for lithium, niobium, yttrium, ytterbium, and scandium.

56Neo-Proterozoic Eratheme

97Vendian System

Neo-Proterozoic sediments, distinguished in Vendian System, are developed in the western part of map sheet M-35-XXII. They comprise the marginal part of the thick terrigenous-volcanogenic sequence developed along the western and south-western slopes of Ukrainian Shield from the border with Belorus to the Black Sea area. The rocks lie over eroded surface of crystalline basement, gently plunging to the west and south-west. In the map sheet area development of Vendian sediments had occurred at the junction between two regional paleo- structures – Podilskiy uplift of Ukrainian Shield and Volyno-Podilskiy trough (VPT). This caused transitional mode of their lithology, in the lower part first of all. In the direction from north to south the progressive change of mainly volcanogenic column, typical for VPT, by the terrigenous one, typical for Podilske Prydnistrovya. At the pre-Mesozoic – pre-Cenozoic surface Vendian sediments are traced along the western border of map sheet in the sub-longitudinal band from 4 km wide in the north to 20-22 km in the south. Their surface altitudes vary in the range from +207 m to +260 m ascending in the south-western direction. On the background of the noted ascend the relatively uplifted and subsided surface sites are noted which can be related either to various activity of individual blocks or to the variable rock lithology that underwent erosion in Mesozoic- Cenozoic. Thickness of the sediments does regularly increase in the western and south-western directions attaining 133.9 m. The patterns of the crystalline basement surface considerably affect the thickness and lithology of Vendian sediments, especially their nasal part. In paleontological respect the Vendian sediments in the map sheet area are not characterized but their similarity with the stratotypical columns in Podilske Prydnistrovya, containing numerous fauna remnants (Metazoa) and micro-phytofossil complexes, make possible the age definition for specific horizons and perform correlation with other regions. The System sediments are ascribed to Lower Vendian Volynska Series and Upper Vendian Mogyliv- Podilska Series. In spite of irregular lithology of Volynska Series, amount of defined litho-stratigraphic units and regularities in their distribution, the rocks are ascribed to two litho-tectonic zones – Khomorska and Pivdennobuzka. In Khomorska LTZ, Volynska Series includes Prygorynska and Slutska suites which, in turn, are divided into (from bottom to top) into Khomorski and Babynski layers in the first case, and Novoselski and

29 Krasylivski layers in the second case. In Pivdennobuzka LTZ Volynska Series is comprised of Grushkynska Suite divided into Bakhtynski (lower) and Vinkivetski layers. Bakhtynski layers are correlated with the middle-upper parts of Babynski layers, and Vinkivetski layers – with Slutska Suite. In Mogyliv-Podilska Series two suites are distinguished: Mogylivska (Olchedaivski, Lomozivski, Yampilski, Lyadivski layers) and Yaryshivska (Bernashivski and Bronnytski layers). The latter layers in the given map sheet are not intersected but mapped close to its southern border in the adjacent map sheet M-35- XXVIII (Bar).

Lower division

Laplandian horizon

Volynska Series

The Series is composed of terrigenous-volcanogenic rocks and lies directly over crystalline basement. With unconformity it is overlain by Olchedaivski sandstones of Mogylivska Suite. Nevertheless, over most part of its distribution area it is exposed at pre-Mesozoic – pre-Cenozoic surface. In the given area Volynska Series is transitional in term of lithology. Most notable changes in lithology are observed in the area between Sluch and Buzhka rivers. In the band 12-16 km wide, in the direction from north to south, amount of clastic material, characteristic for the erosion products of crystalline basement, does strongly increase. Transitional rocks of mainly terrigenous composition are traced in the south-western direction in the distinct rim along the northern slope of Podilskiy uplift of Ukrainian Shield.

Prygorynska Suite (V1pg)

It is developed in Khomorska LTZ where Khomorski and Babynski layers are distinguished. The total thickness of the Suite is up to 82.9 m.

Khomorski layers (V1hm)

Khomorski layers comprise the oldest sedimentary rocks of the cover in the studied area. Their stratotypical column is described in the map sheet M-35-XXI. The rocks are mapped in the north-western part of the area. The eastern boundary of their distribution is set in 1.2 km to the west from Koskiv – Gubcha – Dubyna villages – eastern outskirt of Myrolyubne village and further to the south-west through Novoselytsya, Pashutyntsi, Klymashivka villages. The southern boundary of Khomorski layers is conventional enough and is defined, in our mind, by the development of the basal batch of Babynski layers composed of oblique-banded aleuro-pelitic tuffs. Khomorski layers lie over eroded surface of the crystalline basement and actually everywhere are overlain by Babynski layers, except the narrow band (0.8-1.2 km wide, in places up to 3 km) along the eastern boundary of their distribution, where they are exposed at pre-Cenomanian surface. Khomorski layers consist of the feldspar-quartz, red-brown, diverse-grained, mainly coarse-grained, often clayey sandstones. The clastic material is weakly rounded and sorted. Sandstones often contain 0.7-1.1 m thick interbeds of red-color mica argillites. Somewhere sandstones become light-grey because of considerable kaolinite content and are close to arkoses in composition. These varieties are mainly developed in the band of Khomorski layers exposure at pre-Mesozoic surface (DH 1,2,3). High enough kaolinite content in the rock can be explained by the ancient kaolinite weathering crust the sediments were derived from, or by the post- sedimentation processes of kaolinitization under influence of aggressive groundwaters. In the lower part of the layers the basal breccia, gruss-stones and gravelites are normally observed composed of the granitoids, quartz, feldspar fragments cemented by ironiferous-clayey material. Accessory minerals include garnet, monazite, zircon. High enough concentrations of radioactive element carrying minerals cause increased gamma-activity of the rocks making them reliable geophysical marker. Thickness of sediments varies in the wide range from 1-3 m in the south to 8-12 m in the north-west where the rocks fill up depressions in the relief of crystalline basement. Khomorski layers are perspective for discovery of radioactive and rare-earth raw material deposits confined to the basement-Vendian unconformity. It is thought that Khomorski layers comprise the product of eluvial-deluvial reworking of the basement rocks. According to the valid stratigraphic scheme the rocks are correlated with the upper part of Gorbashivska Suite developed to the north-west in VPT.

30 Babynski layers (V1bb)

Under this name O.V.Krashenynnykova (1956) had distinguished the sequence of tuffogenic sediments in Volyno-Polisskiy trough (after Babyn village in Rivnenska Oblast). Babynski layers are developed in Khomorska LTZ where they lie over Khomorski sediments and are overlain by Krasylivski layers and Meso- Cenozoic sediments. The surface altitudes of Babynski layers descend in the south-western direction from +240…+245 to +185…+190 m. The boundary with underlaying Khomorski layers is normally clear and set by the footwall of distinct tuffite batch occurring at the bottom of Babynski layers and is widely developed over the area. Tuffites are of basalt composition, dark-grey, in the lower part iron-enriched, fine-grained, with thin horizontal and oblique banding, under mixed chlorite-opal cement, up to 10-12 m thick. This tuffite batch in the given area comprises the most persistent volcanogenic layer and can be used as the marker in definition of Babynski layers distribution boundaries since the overlaying rocks are variable in lithology. Tuffites normally exhibit decreased gamma- activity in comparison to the underlaying and overlaying sediments. The rocks, characteristic for the stratotype columns of Babynski layers, are mainly developed in the north-western part of the given LTZ and include dark-grey, greenish-dark-grey, brown, often weakly cemented tuffs and tuffites. Their texture is mainly psammitic, diverse-grained, rarely aleuritic and psephitic. The course- grained varieties predominate. Brown coloring is characteristic for the rocks at the column bottom. The rocks are often layered. The tuffs are litho-vitroclastic in composition. The clastic material includes basalts, felsites and volcanic glass in various proportions. Volcanic glass predominates, especially in aleuritic varieties. The fragments are rounded, with smoothed edges, often irregular. Cement is opal, chlorite-opal, ironiferous-chlorite. Thickness of tuffogenic sediments attains 52 m. Occurrence of opal cement and layering suggest for the sediments development in the water environment with re-deposition of volcanogenic material under its insufficient transport. In the southern direction the tuffs and tuffites are substituted by volcanomictic sandstones and gravelites which keep green-grey and brown coloring while the layering becomes more prominent because of alternating layers with different granulometric composition. Volcanomictic sandstones contain up to 70-80% of fragments. Their shape is semi-rounded, often acute, which is more characteristic for the feldspar fragments. In composition, the fragments are mainly composed of volcanics, quartz, feldspars, rarely granitoids and gneisses. Cement is limonite-chlorite, chlorite-halloysite, opal, chlorite-opal, in places kaolinite, carbonate. Cementation type is basal, porous. Thickness of Babynski layers attains 78 m. Significant thicknesses of tuffogenic rocks suggest for mainly explosive activity in Volynskiy time related to the volcanic centers in the axial part of VPT. Babynski sediments in the southern direction are gradually substituted by terrigenous Bakhtynski layers. The latter in age do apparently correspond to the formation time of the middle-upper part of Babynski layers. The rocks were developing in the shallow-water basin zone under stable tectonic conditions at the beginning of sedimentation and some tectonic activation later on.

Grushkynska Suite (V1gr)

It is distinguished in Pivdennobuzka LTZ. For the first time in the studied area Volynska Series sediments of Grushkynska Suite are mapped in the course of DGM-50 of map sheet M-35-91-D [51]. Correlation with the Suite columns, encountered during GM-50 in the map sheet adjacent from the south, has revealed similarity of their lithological-facial composition, mainly of terrigenous kind. In the Suite two parts are distinguished: mainly clastic – Bakhtynski layers (lower) and clayey Vinkivetski layers (upper).

Bakhtynski layers (V1bh)

They are developed in the south-western part of the area. The rocks lie directly over crystalline basement. Their distribution boundaries are defined by the basement surface morphology. With the azimuth (?) unconformity they are overlain by Vinkivetski argillites. At the pre-Mesozoic – pre-Cenozoic surface the rocks are developed in the band from 9 km wide and up to their complete disappear beneath overlaying sediments. The distribution boundary is set by line: Novoselytsya village – 2 km to the east of Gnativtsi village – Yaroslavka village – Pirogovtsi village – 2 km to the west of Goloskiv village – 1 km to the east from Bogdanivtsi village. The rock surface altitudes vary from +240 m in the east to +136 m in the south-west. The layers are mainly composed of sandstones, gravelites and conglomerate-breccia. Sandstones are feldspar-quartz, in places polymictic, brown, greenish-grey, diverse-grained, mainly medium-coarse-grained,

31 fine-gravel, often with horizontal and oblique gradual banding, somewhere clayey. Sandstones are composed of semi-rounded, often acute fragments of grey and blue quartz (up to 50%), grey, pink-grey, yellowish feldspars (30-35%), with minor pink granite grains and biotite. Cement (15-20% by rock volume) is hydromica-kaolinite, ironiferous (often contains up to 15-20% of iron hydroxides). In the drill-hole columns sandstones are replaced downward by gravelites and conglomerates of the same composition where the fragments of various granitoids and gneisses are observed. Directly above the basement rocks 1.5-3.0 m thick sedimentary breccias are often observed composed of the coarse actually non-rounded fragments of crystalline rocks 2-4 cm in size, rarely up to 10-12 cm across, under sand-clayey cement, red-brown. The fragment shape and composition indicate their insufficient transport and identity to the basement rocks of the given area. In the transitional zone from Bakhtynski sediments to Babynski rocks sandstones of mainly feldspar- quartz composition contain admixtures of volcanogenic material (up to 15%). The interbeds of sandy argillites 0.5-0.8 m thick are also noted. Thickness of Bakhtynski layers is fairly variable since the rocks fill up negative basement relief forms of erosion-tectonic origin. This is well expressed in the borehole profile drilled in the South Boug valley. Maximum thickness of sediments is 48.8 m. From the thickness analysis of Grushkivska Suite, in general, and Bakhtynski layers, specifically, and hydrographic features of the territory, the South Boug valley does apparently coincide with the north-west- trending fault zone. The age of layers is defined from their position in the column and rock composition. Their development had occurred under conditions of arid climate, in the coastal (?) zone of water basin which covered subsided and fault-broken marginal part of Ukrainian Shield.

Vinkivetski layers (V1vn)

These are developed in the north-western part of the area. In the northern direction they are connected by gradual transition with Slutska Suite and together with the latter do comprise the single geological body (Fig. 2.1). Vinkivetski layers transgressively lie over Bakhtynski layers and are unconformably overlain by Olchedaivski layers, and in case of their lacking – by Mesozoic-Cenozoic rocks. The layers are intersected by some drill-holes making possible to examine changes in their lithology by strike. The sediments comprise thin horizontal or slightly-wavy and in places oblique intercalation of grey with greenish and bluish shade, brown at the bottom argillites and light-grey, micro-fine-grained feldspar-quartz sandstones, often lens-shaped. Thickness of interbeds is 1-5 mm, rarely more. The rocks are micaceous at the bedding planes. They contain one-three 0.1- 0.3 m thick interbeds of medium-coarse-grained fine-gravel feldspar-quartz sandstones composed of weakly- sorted and rounded in various extents fragments; among the latter some pebbles of pink pegmatoid granites up to 5 cm in diameter and garnet grain accumulations are observed. The number of sandstone interbeds decreases downward. At the column bottom the batch 3.9-6.6 m thick is observed composed of unclear-banded, green-grey, red-brown argillites with minor clastic, actually non-rounded material. Thickness of the layers increases in the southern direction attaining 47.4 m. In the same direction the column of Vinkivetski layers becomes more sandy and this is well expressed in the adjacent territory where thicker sandstone batches appear in the upper column part. Vinkivetski sediments were developing in the sea basin separated from the west by the basalt plateau or the chain of islands, under conditions characteristic for the bays, lagoons, and underwater depressions.

Slutska Suite (V1sl)

For the first time it is distinguished in the course of DGM-200 in the territory of map sheet M-35-XXI (Khmelnytskiy) where it is comprised of the sandy-clayey sequence which unconformably lies over volcanogenic Babynski layers and with erosion is overlain by Olchedaivski sandstones. In the given territory the unit is mapped in Khomorska LTZ where complete contiguous Suite columns have shown their lithological similarity with the stratotype ones with some distinctions. The eastern distribution boundary of the Suite is set up (from the north to south) by the line of inhabited locations Bovkuny – Rosolivtsi – Movchany – Veselivka. To the south from Pashutyntsi – Klimashivka villages the Suite is connected by gradual transition with its age analogue – Vinkivetski layers of Grushkynska Suite. Thickness of the Suite attains 35.2 m with the general trend for increasing in the south-eastern direction (see Fig. 2.1).

M - 35 - XXI M - 35 - XXII

3601 3600 3608 3606 31.2 29.5 ora 30.8 31.0 Khom 30 3603

3621 27.0 2

26.5 a 5 3631 or 3604 om 3 60 5 3616 20.0 h 29.7 K 3617 19.9 28 .3 26.8 3615 0 3 3 62 2 29.1 3612 25.6 18.0 12612 19.6 20 3611 3 61 3 31.3 21.5 3607 649 32 .7 30.8 3 60 9 3619 34.3 3614 18 24 0 29.0 31 .5 3620 23 . 0 34.6 Starokostyantyniv

3624 8 3627 27 . 7 11. 0 26 .5

5 0

15 10 2

3618 1 09 2 4 ch 0 41.5 17 . 1 Slu 3623 3625 30 12609 35 30.1 30 8 34.3 29 16941 Krasyliv 30 16942 3 629 31.5 32.6 36.6 30 1 69 43 31.0 36 74 25.8 3633 112 34 . 0 37.3 20.3 3676 3653 27.0 33 .5 30 36 73 15.0 36.8 3649 35 12 6 0 6 36.1 31 . 0 17 3 64 7 3639 35 .2 12 34 .7 27.0 31.0 Ch orn iy Ostriv

S out 46 h B ou 3671 35.3

3654 g 44 . 9 4

0 40.1

3661 Khmelnytskiy 4

4 29.8 5 291 85 36.5 26.0 15 1823 7 38.0 14 14.3 18.8 3 659 3670 1823 8 129 43.0 43 .3 45.6 47.4

1 : 500 000 5 kilometers in 1 centimeter km 5 0510 15 km

Thickness scale (m)

0 10 20 30 40 50

3647 0 123 4 5 67 3 31.0

Fig. 2.1. Isopach map for Slutska Suite and Vinkivetski layers in the northern slope of Podilskiy uplift in Ukrainian Shield. 1 – isopachs; 2 – drill-holes intersected sediments of Slutska Suite and Vinkivetski layers: in numerator – drill-hole number, in denominator – thickness of sediments in meters; 3 – boundary of sediments; 4 – boundary of overlaying Olchedaivski layers; 5 – eastern boundary of Slutska Suite basalts; 6 – band of partial sediments erosion; 7 – probable tectonic breaks influenced sedimentation.

33 In the Suite Novoselski (lower) and Krasylivski layers are distinguished, which are observed at the pre- Mesozoic surface in two parallel bands 1.0-2.3 km wide. Tectonic features, distribution and thickness of the Suite are very similar to those of some horizons in Mogyliv-Podilska Series, specifically, overlaying Olchedaivski layers.

Novoselski layers (V1nv)

The stratotype columns of Novoselski layers are encountered in the northern part of map sheet M-35- XXI (Khmelnytskiy) in the area of Nove Selo village. The layers consist of red-brown, dark-brown, brown, fine- mica argillites, often with thin interbeds of light-grey sandstone from some mm up to 10-12 cm thick, rarely more. Some interbeds are often grey-green, bluish-grey in color. In the studied area Novoselski layers comprise intercalation of diverse-color (brown, greenish-grey, bluish-grey) argillites. Thickness of individual interbeds is from 2-3 to 5-10 cm, rarely up to 1 m. The brown coloring predominates in general. Argillites are micaceous, with thin horizontal banding, which is often highlighted by thin (first mm) interbeds of fine-grained sandstones. In addition, 1-2 interbeds are noted from 3-5 cm to 30 cm thick of feldspar-quartz coarse-grained sandstones, in places with feldspar gravel and pebble. The total thickness of sediments attains 18.1 m. It should be noted that brown-coloring intensity in Novoselski sediments decreases from the north to south and is apparently related to the underlaying rock composition. Novoselski layers lie over Babynski layers with unconformity which is not always clear and is marked by thin basal gravelites. The boundary with overlaying Krasylivski layers in not clear and is set by the rock brown color disappearing and increasing number of sandstone interbeds. The rocks are not characterized in fauna. The age is defined by the position in column and rock lithology. Novoselski layers by their lithology can be correlated with the lower brown-color part of Vinkivetski layers.

Krasylivski layers (V1kr)

The rocks, which correspond to Krasylivski layers of Volynska Series, were distinguished for the first time in 1971 by A.M.Khanysenko in the area of Krasyliv village and studied in details in the course of DGM- 200 in the map sheet M-35-XXI. In the stratotypical column nearby Chernelivka village of Krasylivskiy area in Khmelnytska Oblast the batch of 19.0 m total thickness is intersected composed of greenish-dark-grey argillites with thin horizontal banding, low-mica, with few up to 0.2-0.5 m thick interbeds of coarse-grained arkosic sandstones. In the given map sheet M-35-XXII Krasylivski layers by their lithology do correspond to the stratotypical columns. These are mainly grey, dark-grey, often with greenish shade, fine-mica argillites with horizontal and slightly-wavy banding caused by thin (1-5 mm) crosswise and lens-shaped interbeds of light-grey feldspar-quartz fine-grained sandstones. Single interbeds up to 5-10 cm thick of the coarser-grained arkosic sandstones are also observed. Thickness of the sediments is up to 17.1 m. The boundary with overlaying Olchedaivski sandstones is sharp and marked by the change in lithology. To the south Krasylivski layers are gradually replaced by Vinkivetski layers and can be correlated with their upper part. The rocks are not characterized by fauna although in adjacent territory the complex of micro-fossils is determined in these sediments, typical for the upper part of Volynska Series, making possible their correlation with the rocks of Grushkynska Suite in Podilskiy uplift of Ukrainian Shield. Novoselski and Krasylivski layers were developing under coastal conditions of the narrowed water basin.

Upper division

Redkinskiy horizon Mogyliv-Podilska Series Mogylivska Suite (V2mg)

In the Suite the Olchedaivski, Lomozivski, Yampilski and Lyadivski layers are distinguished and mapped in the north-western part of the map sheet. Their exposures at pre-Mesozoic surface are extended in the sub-parallel bands in the north-north-western direction. Complete column of the Suite is only intersected by the drill-hole nearby Shumivtsi village [47].

Olchedaivski layers (V2ol)

The eastern layers boundary is set by line of Berezova – Chervona Zirka – Pechesky – Shryborivka – Lagodyntsi villages (Fig. 2.2). The band width of layers exposure at pre-Mesozoic surface is 3-6 km. The layers surface altitudes vary in the range from +198.1…+259.5 m with descending trend in the western and south- western directions. However, along the South Boug river valley the altitudes are steady in the range +240.0…+245.0 m. Perhaps, it is resulted from the motions of individual tectonic blocks. Olchedaivski sediments unconformably lie over argillites of Krasylivski and Vinkivetski layers. In the studied columns the boundary definition between the units is not complicated. However, with appearance of thick sandstone interbeds in Vinkivetski layers the possibility appears to include the upper part of Grushkynska Suite into Olchedaivski layers making their thickness much higher abruptly. This can explain the overestimated (up to 50-54 m) thickness of Olchedaivski layers reported by A.M.Khanysenko in the course of DGM-200. In general, the thickness of Olchedaivski sediments both in the studied and adjacent territories in the complete columns rarely exceeds 20-25 m. The layers are mainly composed of grey, light-grey, in places yellowish feldspar-quartz sandstones, coarse-grained at the bottom, with minor fine gravel. Higher up the column the rocks become coarse- and medium-grained and gradual banding is often observed. Somewhere lower column part is composed of alternating grey-green argillites and fine-grained sandstones. Sandstones are composed of semi- rounded and rounded quartz and feldspar (mainly potassium) grains. Cement is kaolinite, hydromica in composition, rarely calcite in various combinations. Paleontologically the rocks are not characterized. Their formation occurred under conditions of river valleys and their deltas. Litho-facial features of sediments suggest that in the beginning of Mogyliv-Podilskiy time climatic conditions had been drastically changed form arid to warm and wet. This has facilitated weathering crust formation in the source regions and appearance of kaolinite in sandstones.

Lomozivski layers (V2lm)

These are developed to the west from line Kolyban – Stufchyntsi – Zaruddya villages (see Fig. 2.2). The rocks are traced in the sub-longitudinal band from 2.0 km wide in the north up to 5 km in the south beneath Mesozoic-Cenozoic sediments. Sediments gently plunge down in the western direction. The surface altitudes are in the range +210…+247 m. Thickness attains 21.5 m in the contiguous columns. The composition is persistent. The layers comprise thin horizontal intercalation of grey, greenish-grey, rarely brown aleuritic argillites and aleurolites, in the lower part with interbeds of grey, light-grey, fine-grained sandstones. Argillite composition is kaolinite-quartz-hydromica. Texture is politic, crypto-flaky. Sandstones are feldspar (10-15%) – quartz (70-75). In the stratotypical columns in Prydnistrovya Lomozivski layers contain numerous remnants of spineless fauna indicating their formation in marine basin.

Yampilski layers (V2lm)

The layers column is intersected by the only DH 18238 [46] nearby Shumivtsi village. However, in view of geological mapping data obtained in adjacent territories from the south and west, and the general regional persistent lithology of this straton, the distribution area of these sediments can be bounded by the line of inhabited localities Lugove village – eastern outskirt of Khmelnytskiy town – Pyshkivtsi village – Veremiivka village. The width of sediments exposure at pre-Mesozoic surface is 3-5 km. In contrast to the stratotypical columns, mainly composed of sandstones, in the studied area Yampilski layers are three-folded: at the bottom – feldspar-quartz, light-grey, fine-grained sandstones with carbonate- clayey cement; higher up – thin horizontally-wavy intercalation of light-grey sandstones and aleurolites, which then are overlain by the batch of green-grey argillites. The total thickness is 30.8 m. The boundary with overlaying argillites of Lyadivski layers is not clear because of similarity in lithology between the units. By strike to the north, in adjacent map sheet M-35-XXI, the fully clayey columns of these layers are observed. Sandstones are mainly composed of quartz (70-80%) and feldspar (20-30%). Argillites are hydromica- quartz-kaolinite with minor clastic material. In the studied area the rocks are not characterized by fauna. The sediments were developing under marine basin conditions away from the clastic material source regions.

M - 35 - XXI M - 35 - XXII 1 80 1 17 0 3660 650 3602 7.0 60 3608 1 135.5 70.8 60.2 ora 3601 101 2 hom 161.3 3606 K 148 23.1 5.8 148.3 3603 3621 0 383 15 Khomora 148.6 150 50.0 3616 3631 36 05 322 3604 3615 391 3 157.3 148.5 14 3.5 8.0 157.3 125.3 53.0 29.4 12610 364

142.5 0

9 425 3611 0 3.0

8 436 15 01501501501501501501501501501501501501501501501501501501501501501501500 0 50.0

3612 12612 7

136.6 0 62.0

2 0

134.5 1

149 1 345 1 0 1 307 18.0 40.0 3607 301 124 3613 139.2 23.9 0 8.5 137.4 14 3609 328 11 3 Starokostyantyniv 132.5 3620 18240 72.0 588 30 23.5 3614 1 129.3 104.1 589 40.7 11 1 3619 133.5 30.0 139.1 42.0 596 S 3627 37.3 590 luc h 129.5 14.7 36 24 8 344 3618 133.0 9 10 92.9 6 135 3623 40.6 26.5 141 140 130 3625 568 12609 16941 132.0 26.0 127.4 120 125.5 3675 3629 130.5 Krasyliv 116.5 30 19 11 3.2 56.1 18226 9.5 16943 570 3656 3653 3674 120.9 123.5 130.7 35.0

122 0

2 0 1

1 0 1

120 0

3633 0

9 8

3673 0

117.5 7 6

123.3 0

0 5

306 4 12606 12 0 3 17 98.8 67.0 308 0 110 3649 125.3 2 3639 58.9 0 11 9 116.3 18239 1 114.8 3647 18.6 106.1 Chorniy Ostriv 11 3 B 5.7 uz 3654 ho 103.7 S 46 1235 k ou 17.0 th B 88.0 ou 3671 3669 g 1564 118.9 110.3 90 11 6 10.0 Khmelnytskiy 75 90.5 15.8 96.6 0 88 9 85 80 75.5 29 297 75 7 106 49.3 0 365 9 65 3666 60 14 1253 0 108 301 123.0 12 18238 299 27.9 45.9 0 51.6 303 158 8

11 77.2 59.3 1

85 0 64.0 203 4 100 3670 0 129 93.0 1598 11 76.3 90 8.6

1 : 500 000 5 kilometers in 1 centimeter km 5 0105 15 km

Thickness scale (m)

0204060 80 100 120 140 160 180 200

0 3671 100 1 110.3 2 345 6

Fig. 2.2. Isopach map for Vendian Volynska Series and Olchedaivski layers of Mogyliv-Podilska in the northern slope of Podilskiy uplift in Ukrainian Shield. 1 – isopachs; 2 – drill-holes intersected Volynska Series and Olchedaivski layers: in numerator – drill- hole number, in denominator – total thickness of sediments in meters; 3 – boundary of Volynska Series; 4 – boundary of overlaying Lomozivski layers; 5 – band of partial sediments erosion; 6 – probable tectonic breaks influenced sedimentation.

Lyadivski layers (V2ld)

In the given map sheet they only include the lower column part, specifically, brown, greenish-grey argillites 4.4 m thick. Complete contiguous column of the layers is described in 1.4 km to the south, in adjacent territory, in DH 4282 [14]. Lyadivski sediments conformably lie over Yampilski layers and with erosion are overlain by Bernashivski sandstones. The sediments surface altitudes are +250…+255 m. In general, the layers are persistent in lithology in adjacent territories from the west and south. Normally, at the bottom these are green, grey-brown argillites, and at the top – brown, fine-mica, fine-fracture argillites, thin-banded due to diverse-color 1-2 cm thick interbeds. Somewhere thin (up to 1 cm) interbeds of fine-grained feldspar-quartz sandstones are observed in the lower and middle column parts. Thickness of the layers varies from 4-5 to 18 m. Characteristic argillite texture is thin-flaky pelitic. Rock composition is chlorite-quartz-hydromica- kaolinite with strong kaolinite predomination. The age of layers is defined by their position in the column. Sedimentation had occurred in the shallow- water basin with evidences for stagnation and sulfur hydrogen enrichment.

Yaryshivska Suite (V2jr)

The Suite rocks are not described in the studied map sheet area but, taking into account the Suite distribution in adjacent territories, development of these sediments is possible in the far south-west of the given map sheet. Bernashivski (lower) and Bronnytski layers are distinguished in the Suite.

Bernashivski layers (V2bn)

The rocks are studied in adjacent territories from the west and south, including the area in direct proximity to the southern map sheet margin where they are described in the course of GM-50 [14]. Bernashivski layers with erosion lie over Lyadivski layers and are conformably overlain by Bronnytski layers; in the band of their exposure at pre-Mesozoic surface they are overlain by Lower Cretaceous glauconite- quartz sands. The layers column in the region is normally two-folded. Specifically, to the south (DH 4282) [14], in the lower part they are composed of greenish-grey, feldspar-quartz, fine-grained sandstone, medium-grained in the interbeds, high-clayey, which upward is gradually replaced by grayish-green, banded aleurolites and aleuro- argillites with thin (up to 10 cm) interbeds of clayey sandstones. Sandstones are composed of quartz (80%) and feldspars (up to 20%) with noted chlorite, pyroxene, glauconite. Thickness of the layers is up to 16.4 m and in the western direction it decreases up to 6-8 m. The age of sediments is mainly defined by their position in the column. In the stratotypical columns of Prydnistrovya Bernashivski layers contain spineless fauna. Their development had occurred under conditions of shallow-water sea and its bays, as it is evidenced by glauconite occurrence and rock banding.

Bronnytski layers (V2br)

In the studied map sheet these layers are not encountered. They are mapped in adjacent territories from the south and west. Their occurrence is possible in the far south-western part of the given map sheet. By analogy with adjacent territories, it is assumed that Bronnytski layers conformably lie over Bernashivski layers and with erosion are overlain by Cretaceous sediments. Two batches are being commonly distinguished in the layers. The lower one is composed of massive or unclear-banded, dense, siliceous, red-brown argillites originated through the tuffogenic material re- crystallization. The upper batch consists of chocolate-brown, brown-green, fine-mica argillites, often crushed to the fine debris. In these rocks material of volcanogenic origin is also found. Thickness of the layers attains 7 m and more. The age of sediments is defined by their position in the column and distinct lithology. Development of the rocks had occurred under conditions of marine basin shortening with volcanic ash material input, apparently from the Dobrudja area [29].

PHANEROZOIC

22Mesozoic Eratheme

57Cretaceous System

In the studied area Cretaceous sediments are only developed in the western part, in the slope of Ukrainian Shield. By analogy with adjacent territories, where the System column is more completed and sediments contain the leading fauna remnants, and taking into account the stratigraphic position and rock lithology, the Pylypchanska and Ozarynetska suites are distinguished. The first one is Cenomanian and the second one – Turonian of Upper Cretaceous.

98Upper division

Cenomanian stage

Pylypchanska Suite (K2pl)

The distribution boundary of Pylypchanska Suite is set in the north-north-western direction through the inhabited localities Masivtsi – Redvintsi – Myrolyubne – Starokostyantyniv – Grybenynka – Zalissya – Vyshneve. In the Suite distribution area erosion sites are observed at Lagodyntsi, Rosolivtsi, Pecheski villages and to the west from Zhovtneve village (Fig. 2.3). The Suite is not exposed at the surface. The Suite is composed of glauconite-quartz sands and sandstones with flint concretions. The rock footwall altitudes vary from +207.7 to +255.3 m. Maximum Suite thickness attains 13.1 m (Verkhnyaky village area), average – 7-8 m. Pylypchanska Suite with angular unconformity lies over Upper Precambrian rocks and is overlain by Ozarynetska Suite, and in places where the latter is lacking – by Paleogene Kyivska and Obukhivska suites. In the Suite column minor differences are established in the composition and structure of lower and upper parts. In the lower part, commonly close to the footwall, the glauconite-feldspar-quartz sandstones are noted, greenish-grey, diverse-grained, mainly medium-grained, in places with little gruss admixture; higher up these rocks are replaced by finer-grained, greenish-grey, grey glauconite-quartz sands and sandstones with carbonate-clayey cement, where flint concretions 5-7 cm in size are noted in places. The upper part (0.3-4.0 m thick) is composed of quartz-glauconite and glauconite-quartz, dark-brown-green, fine-micro-grained, often clayey sands with flint concretions up to 15-20 cm in size. Glauconite content in the upper part is higher than in the lower one. By results of pan-sample mineralogical analysis, the following concentrations are determined in Pylypchanski sediments (kg/m3): pyrite – up to 2.54, glauconite – up to 1.0, apatite and callofane – up to 0.48, tourmaline – up to 0.08. In minor and trace amounts ilmenite, zircon, monazite, chalcopyrite, pyrrhotite and pyrope are noted. By chemical analysis in quartz-glauconite sands from the upper column part of Pylypchanska Suite the P2O5 content is determined in the range 3.42-5.85% (Pyrogivskiy and Goloskivskiy apatite occurrences). By the position in column, lithology, mineral composition, flint occurrence and coloring, the sediments are correlated to the fauna-supported (Gavelinella cenomanica Brotz., Arenobulimina sabulosa Chapm.) Cenomanian sediments mapped in adjacent territories [13].

Turonian stage

Ozarynetska Suite (K2oz)

Like Pylypchanska Suite, Ozarynetska Suite is exclusively developed in the western slope of Ukrainian Shield where it is known almost everywhere. It is eroded also at the same site as Pylypchanska Suite. The Suite boundary is sub-parallel to the boundary of Pylypchanski sediments (in 0.5-4.0 km to the east) and is caused by the relief of pre-Cretaceous surface. Ozarynetska Suite lies over Pylypchanska Suite and in places where the latter is absent – over Upper Precambrian rocks, and just to the east from Pyrogivtsi village – over basement rocks. It is overlain with erosion by Paleogene Kyivska and Obukhivska suites, and in places where the latter are lacking – by Sarmatian sediments.

2 2 1 Khom 6.6 ora

S 2 ) Grytsiv lu c 5.7 h

V erb ka

3 a Lyubar ilk Kpl 7.6 B 1-2 a chk evy 178 Der 4.2

177 teriv

3.3 Te

2 Biluga 2 0

4 0 P 18240 opi v 7.0 ka Ikopot 0 4 Starokostyantyniv 2

G 10 ra b 9 a 9.5 rk 11.8 a

10 h Sluc

172 10 13.1 19 30 240 8.2 0.3 Do ma Koz kha 2 107 Ikva 2.6 Stara Synyava

130 KHMILNYK 2.6

17 0

Buzhok 24

12.5 0 10 1

18239 g

u 13 13.0 o B Kudynka

h 13.8 t 113 N u ovo o 5.1 sta S vts i L ake 0 5 2 Fosa Medzhybizh 2 4 0 ug 2 Bo 5 h 0 ut So 15 18237 14 0 7.4 1.3 5 5.1 2 Letychiv 40 vk 2 Vo 18238 10 11.1

1 : 500 000 5 kilometers in 1 centimeter km 5 0105 15 km

1 2 3 456 10 7 220 8

9 11.8 9 10 11

Fig. 2.3. Distribution sketch of Ozarynetska (K2oz) and Pylypchanska (K2pl) suites in the map sheet M-35- XXII (Starokostyantyniv). 1 – distribution of Ozarynetska Suite; 2 – distribution of Pylypchanska Suite, not overlain by Ozarynetska Suite; 3 – buried area of Pylypchanska Suite; 4 – boundary of Cretaceous System; 5 – buried boundary of Pylypchanska Suite; 6 – boundary of Pylypchanska Suite, not overlain by Ozarynetska Suite; 7 – isopachs of Cretaceous sediments; 8 – footwall isohypses of Cretaceous sediments; 9 – drill-holes: in numerator – drill-hole number, in denominator – thickness of Cretaceous sediments; 10 – probable tectonic breaks; 11 – area of probable erosion of Cretaceous sediments.

The Suite footwall altitudes vary from +210.8 to +256.4 m. Maximum thickness of Ozarynetska Suite attains 11.6 m, average thickness – 2-3 m. At the surface the Suite is not exposed and in the borehole cores it is composed of dark-grey to black flint concretions, with shell fracture, often in the white tripoli “rim”. The contact with Pylypchanski sediments is not identified. In comparison to the stratotypic columns of Ozarynetska Suite, composed of siliceous limestones with Inoceramus labiatus Schloth., tripoli, cobble chalcedonolites of total thickness up to 22 m, in the given area, at the margin of its development, the Suite is much thinner and limestone constituents are absent. The Suite is composed of cobble flints with minor tripoli.

23Cenozoic Eratheme

Pre-Quaternary Cenozoic sediments in the studied map sheet are distinguished in two litho-tectonic zones – Khmelnytska and Berdychivska, where they differ in the column, lithology and structure. Khmelnytska LTZ occupies the western, central and south-eastern parts of the map sheet, and Berdychivska LTZ is developed in the north-eastern part. In Khmelnytska LTZ Paleogene and Neogene columns are mainly composed of marine sediments: Eocene Kyivska and Obukhivska suites, Middle Miocene Podilska suite, thick and most developed batch of Upper Miocene Sarmatian sediments, where three sequences are distinguished – coaliferous sands and clays; limestones; sands and aleurolites – and Pliocene continental sequence of red-brown clays. It should be noted that in Berdychivska LTZ Sarmatian sediments are weakly developed and their stratigraphic relationships with Upper Miocene rocks in this zone is not completely established. Paleogene and Neogene column in Berdychivska LTZ consists of continental sediments exclusively including Eocene Buchatska Series, Lower-Middle Miocene Novopetrivska Suite, Upper Miocene sequence of parti-colored clays, and Pliocene sequence of red-brown clays.

58Paleogene System

99Eocene division

Buchatskiy regio-stage

Buchatska Series (P2bč)

Buchatska Series is developed in Berdychivska LTZ in the eastern part of the area where it fills up Khmilnytska erosion-tectonic depression extended in the north-western direction. Its length in the territory of map sheet M-35-XXII is 23-25 km and width varies from 2.4 to 3.9 km. Depression contours are caused by the surface relief of crystalline basement and is curvilinear. Buchatska Series lies over weathering crust of crystalline rocks and is overlain by the Sarmatian sequence of clays, sands and aleurites. Buchatski sediments are encountered at the depth from 19.5 to 73.0 m. The footwall altitudes vary from +210.4 to 249.0 m. The maximum thickness is 25.4 m (to the north of Berezivka village), the average thickness – 8-10 m. The highest Series thicknesses are confined to the central part of Khmelnytska depression. By composition and sedimentation conditions the river course and flood-land facies are distinguished (Fig. 2.4). The river-course facies is confined to the deepest central part of depression. The river-course sediments include diverse-grained, mainly medium-coarse-grained sands. The sands are mainly quartz, rarely feldspar- quartz, grey, light-grey, in places clayey and coaliferous, with weak grain rounding. Often lignite fragments and minor wood remnants are observed in the sands. In places sands are slightly cemented up to sandstones with clayey and kaolinite cement. The average thickness of river-course facies sands is 4-5 m. After mineralogical analysis results, these sediments contain ilmenite, monazite, garnet, zircon, rutile, kyanite, pyrite. In minor amounts apatite, sillimanite, siderite, tourmaline are noted. The light fraction of sands consists of quartz and feldspar.

M-35-XXII (Starokostyantyniv) Khomora Grytsiv Lyubar

Sluch Maliy Brataliv Starokostyantyniv

Teteriv

P P

P P P P 13898 Stara Synyva P 0.3 P P 33 P 0 KHMILNYK Q 5 P 13.7 2

230

0 P 3 P 2 P P P P PP P P 13970 P P Q 25.4 2 P P P 0 P P 2

30 South Boug

0 0

P 5 1 2 Letychiv P

13937 `P P 9.8 13990 SCALE 1:1 000 000 P P 19.5 P

P P 15161 15202 10.5 1 2 18.8 1597 P 0 15160 3.1 5 2 9.3 P P P P P 3 4 P ` P 1 10 15211 0 3.5 15154 P P P PPP P P P P P P P P P P P P 15163 P P` P P P P P P P P P P P 13.6 P P P P P P P P 15162 PPP P P P P P P P

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P Q 24 15141 0 2 250 11.0 ` 15 18.9 16 ` P 116 1 Q 23.1 0 P 17 18 15209 D 14.5 om ak ha 230 P

15139 PP 8.3 1 - river-course facies: quartz, medium-coarse- grained sands with gravel and pebble, often with

250 lignite and wood fragments; 2 - flood-land facies: fine- and medium-grained sands, often clayey and slightly-coaliferous, coaliferous, in 15771 12.3 places kaolinite clays and aleurites; 3 - KHMILNYK distribution boundary of Buchatska Series; 4 -

g ou facial boundaries; 5 - fine-grained quartz sands; B th ou S 6 - medium-fine-grained sands; 7 - coarse- grained sands with pebble and gravel; 8 - clayey sands; 9 - coaliferous sands; 10 - clays; 11 - coaliferous clays; 12 - kaolinite clays; 13 - secondary kaolines; 14 - isopachs of Buchatski sediments by 10 m; 15 - footwall isohypses of Buchatski sediments; 16 - drill-holes: in numerator drill-hole number, in denominator thickness of sediments in meters, to the left overlaying and underlaying rock indices; 17 - 1 : 200 000 area of probable erosion; 18 - probable tectonic 2 kilometers in 1 centimeter km 2 0 24 6 km breaks.

Fig. 2.4. Lithological-facial map of Buchatska Series (P2bč) in map sheet M-35-XXII (Starokostyantyniv).

The flood-land facies occupies the greatest square. In contrast to the river-course facies, it is quite variable in term of rock lithologies which often alternate in the columns. These mainly include clays, sands and aleurites. In the minor amounts kaoline clays and secondary kaolines are observed. The flood-land facies sands are fine-grained, rarely fine-medium-grained, quartz, coaliferous, often clayey, grey, light-grey, in places with brownish shade. They are observed both in the lower column part, where they overlie coarse-grained sands of river-course facies, and at the column top. Thickness of the flood-land sands is 8-11 m in average. After granulometric analysis results, in the sands the grains 0.25-0.07 mm in size predominate (up to 76%), rarely 0.5- 0.25 mm (about 20%). Clay fraction yield is 2.4-12.7%. The clays are from ash-grey to almost black (depending in coaliferous matter content), often aleuritic and sandy, in places contain coalified plant detritus, rarely – coarse wood remnants. The interbeds of brown- black, coaliferous, micaceous clay 0.5-1.2 m thick are noted. After granulometric analysis, clay particles constitute 85-98%, aleuritic – 0.5-14%, sand – up to 1-2%. Kaolineous clays often by strike, rarely in column, are replaced by coaliferous ones. They are light- grey, grey (depending on coalifying degree), dense, with minor sandy material, rarely coalified plant remnants are observed. Aleurites are developed in the central part of depression. They are observed in the interbeds from 10 cm to 1 m thick within clays and sands. Aleurites are micaceous, mainly brown, more friable than clays, sandy. Total thickness attains 2.8 m. In Buchatski sediments the interbeds of secondary kaoline are scarcely observed, being discontinuous both by strike and thickness. They are normally confined to the upper column part. Thickness of interbeds is 1-2 m in average, maximum – 9.6 m. Secondary kaolines are light-grey, dense, viscous, with minor light mica. The light fraction in kaolines constitutes from 80 to 95% and is mainly composed of quartz. The heavy fraction includes zircon, rutile, kyanite, pyrite, ilmenite, monazite, garnet. Spore-pollen complex, after T.B.Gubkina, contains mainly spermatophyte sub-tropical and tropical plants (Myricacea, Castanea, Trudopollis pompeskyi Pl, Rhus, Hex). Gymnospermous include pine-tree pollen Pinus Diploxylon and Haploxylon. These spore-pollen spectra are typical for Middle Eocene sediments (Buchatska Series) of Ukraine.

Kyivskiy regio-stage

Kyivska Suite (P2kv)

Paleogene sediments in the western slope of Ukrainian Shield of map sheet M-35-XXII previous authors have ascribed in full to Kyivska Suite. However, analysis of data from the map sheet M-35-XXVIII and adjacent areas [1] suggests for development of both Kyivska and Obukhivska suites, which is supported by paleontological data and Paleogene column rock lithology. In the map sheet M-35-XXII Kyivska Suite is developed in the western part, in Khmelnytska LTZ, on the slope of Ukrainian Shield, where it is observed everywhere except the narrow band in the south-western part. To the east from the shield slope boundary Kyivski sediments are preserved in the single “remnant” in the area of Zhabche-Chorna villages (Fig. 2.5). On the shield slope the Suite with stratigraphic unconformity lies over Cretaceous Ozarynetska and Pylypchanska suites, and in places where the latter are absent – over Upper Precambrian rocks. Outside the distribution areas of Cretaceous and Vendian sediments the Suite lies over the rocks of crystalline basement and their weathering crusts. It is overlain mainly by Upper Eocene rocks (Obukhivska Suite), and in places where the latter are absent – by Sarmatian and Quaternary sediments. The Suite footwall altitudes vary from +212.0 to +268.7 m. The maximum thickness of sediments is 17.2 m (Yaroslavka village area), the average – 8-10 m. By lithology Kyivski sediments include mainly clays and marls, in lesser extent – sands and sandstones. The clays are confined to the Suite upper column parts. Their average thickness is 1.0-2.5 m, maximum thickness 8.5 m is noted in 1.0 km to the south-east from Zaruddya village. Clays are often sandy, rarely aleuritic, mainly dense, viscous, non-carbonate or slightly-carbonate, often contain admixture of glauconite, in the lower column parts in places with single gravel (up to 3-5 mm) of quartz and black flint. The marls constitute the lower part of Kyivska Suite. These are grayish-white, light-grey, dense, clayey, diverse-sandy, contain fine dissemination of glauconite in amount up to first percents, in places slightly porous, massive, often with numerous fragments of mollusc shells. In places, where marls directly overlie the older rocks, they contain quartz grains of gravel size. The rocks are mainly composed of calcite (by 60-70%). The

42 clayey fraction includes montmorillonite and kaolinite. Thickness of marls attains 12.9 m (Vyshneve village area).

1 Khomora 101 12.2 S l 16.9 u 2 c Grytsiv h 14.3

10 V erb ka 2 18217 3

3 0 6.2 Lyubar

10.7 4 1 0 0 a chk evy 178 Der 8.5 Bilka

2 103 4

0 3.1

177 Teteriv

7.42 1

0 Biluga 3

2 124

2 12.6

4 0 P op 18240 ivk 7.0 111 a Ikopot

8.8

2 5 0 Starokostyantyniv 18221 G 9 0 2.0 ra

4 b 10 a r 9.0 2 k 7.3 a 109 h 5.3 Sluc

172 2 4 4.1 0

19 0

30 5

5.5 2 18226 D 6.0 om 0.7 ak 112 ha 9.2 107 Ikva

7.9 2

4 Stara Synyava 0

130 9.7 Bu 17 zhok 1 KHMILNYK 11.30 12 0 4 11.3 2 g

B 0 N Kudynka 1 o h v t os tav u tsi o La S ke 46 3.0 1564 250 F osa

7.5 10

50 0

4 2 116 6.8 Medzhybizh g ou B th 291 ou 14 S 15 297 8.7 2.6 18237 0 5.0 3.8 5 Letychiv 2 1593 k v 0.4 o V 2 129 2 6 1597 5 0 1594 1.4 240 7.0 0 0.5 1 : 500 000 5 kilometers in 1 centimeter km 5 0 5 10 15 km

1 0 1 1 2 250 3 12,2 4 5

Fig. 2.5. Distribution map of Kyivska Suite (P2kv) in map sheet M-35-XXII (Starokostyantyniv). 1 – distribution boundaries of Kyivska Suite; 2 – isopachs; 3 – footwall isohypses; 4 – drill-holes: in numerator – drill-hole number, in denominator – thickness in meters; 5 – probable tectonic breaks; 6 – area of probable erosion of Kyivski sediments.

The sands and sandstones are confined to the lower parts of the Suite. The sands are glauconite-quartz, light-grey with greenish shade, fine-medium-grained, clayey, often friable. In places fine gravel of quartz and dark-brown flint is observed. Sandstones, like the sands, are glauconite-quartz, mainly greenish-light-grey, from weakly-cemented to dense, massive, non-layered; in spots, rarely by interbeds, are flinted. In places sandstones are cavernous with minor hollows, somewhere with shell imprints. Often contain minor amounts of rounded, coarse (up to 3 mm) quartz grains. Cement is carbonate-siliceous. Thickness of sand and sandstone interbeds varies from some centimeters to first meters. By the results of micro-fauna studies from marls, T.S.Ryabokon has determined foraminifera complex which corresponds to the zone Hantkenina alabamensis of Kerestynskiy sub-horizon of Middle Eocene Novopavlivskiy horizon. This conclusion is made because of occurrence in foraminifera family the leading zonal species Hantkenina alabamensis Cushman and characteristic for Kerestynskiy sub-horizon plankton (Globigerina apertura Cushman, Acarinina crassaformis (Galloway et Wissle), Globigerina frontosa Subbotina, Globigerinella volluta (White)) and benthos Cibicidoides hadjibulakensis (N. Bykova), Uvigerina proboscidea Schwager, Valvulineria palmarealensis Nuttall, Anomalina atfinis (Hantken)) varieties. Occurrence of mentioned plankton varieties, especially Hantkenina alabamensis, molluscs and nummulites in Kyivska Suite suggest for the tight link of Middle Eocene basin in the area with marine basin of Prychornomorya.

Obukhivskiy regio-stage

Kharkivska Series

Obukhivska Suite (P2ob)

Obukhivska Suite is developed in Khmelnytska LTZ in the western part of studied area, mainly on the slope of Ukrainian Shield. The modern Suite boundary is extended in the sub-longitudinal direction from the south to north by line of inhabited localities Goloskiv – Golovchyntsi – Malomlyntsi – Demkivtsi – Vyshneve (Fig. 2.6). In the slope of Ukrainian Shield the Suite is developed almost everywhere except some minor sites. The Suite transgressively lies over Kyivska Suite, and in places where the latter is absent – over crystalline rocks and their weathering crusts. It is mainly overlain by Sarmatian, rarely Quaternary sediments. The footwall altitudes vary from +228.2 to +271.7 m. Thickness of the Suite is 5-6 m in average, and in relatively subsided sites of pre-Obukhivskiy relief it rises to 18.2 m (Pyrogivtsi village area). Obukhivski sediments were depositing in the shallow-water marine basin existed at the end of Eocene transgression. By lithology and layering patterns they comprise intercalation of sands and sandstones, diverse- sandy clays, in places, where Obukhivski sediments are developed more widely than Kyivski, with the basal horizon composed of the weathering crust erosion products (gruss) and sand-clayey material. The sands are glauconite-quartz, greenish-light-grey, fine-micro-grained, rarely fine-medium-grained, clayey in various extents. Sandstones are glauconite-quartz, mainly greenish-light-grey, massive, non-carbonate, non-layered. Rarely the inter-layer flinting is observed. Cement is clayey-siliceous. In places thin (up to 20 cm) interbeds of silica-clay-like sandstones are noted. Between the sands and sandstones the gradual transitions are often observed. In the sand layers thin lens-like interbeds are often observed which are replaced with sands by strike. The sands and sandstones are mainly composed of quartz, glauconite, feldspar, clay minerals. By results of mineralogical analysis, in sands and sandstones ilmenite, zircon, apatite, pyrite are contained in the weight concentration, and in the sign amounts – corundum, spinel, magnetite. Paleontologically the Suite is not characterized. By the position in column, lithology and analogy with adjacent from the south territory the sediments described above are ascribed to Obukhivska Suite.

2 3 1 0 khomora 8.2 S lu 2 Grytsiv c

4.2 h

i 0 B

4 V erb

2 ka 18217 2 6.3 3 4 Lyubar 0 6.6 a chk 2 revy 30 De 178

5.9

2 0

30 4 0

2 177 1 Teteriv 3.7 Biluga 1 0 124 105 10.510.6

P op ivk Iko a pot 111 5.0 Starokostyantyniv 18221 8 G 6.6 ra b 6.0 9 0 a 1 rk 6.5 2 a 10 5 0 h 11.6

Sluc

1 0 172 11.0 18225 Ikva 9.5

19 0

30 4 9.0 18226 D

2 o 2.0 ma 3.3 kha 112 107 Ikva

5.0

0 6.4

5 2 Stara Synyava 250

130 1.0 B uzh ok KHMILNYK

N Kudynka B ov 113 o h st t av u t o 4.2 si L S ak e 1557

46 26

1 10.5 0 1599

5.8 0 1555 2

6 3.5 1564 0

2 F

6 7.0 os 7.5 0 a 1558 13.8 1556

116 5.0

2.7 Medzhybizh0

192 7

2 1 0 8.7 ug

o 0 B 10 uth 1 297 15 So 12.6 15.7 14 18237

11.0 18.2 270 Letychiv

0 2 1592 k

6 6 ov 2 2 0 V 18238 50 0.8 129 1593 3.0 1597 0 8.7 17.8 6.6 26

1 :500 000 5 kilometers in 1 centimeter km 5 0 51015 km

14 1 10 2 250 3 11.0 4 5

Fig. 2.6. Distribution map of Obukhivska Suite (P2ob) in map sheet M-35-XXII (Starokostyantyniv).

1 – distribution boundaries of Obukhivska Suite; 2 – isopachs; 3 – footwall isohypses; 4 – drill-holes: in numerator – drill-hole number, in denominator – thickness in meters; 5 – probable tectonic breaks.

59Neogene System

100Miocene division

Badenian regio-stage

Podilska Suite (N1pd)

Podilska Suite in the map sheet M-35-XXII is locally developed in the southern part of the area in Khmelnytska LTZ, on the right and left banks of Vovk river. It is weakly studied and intersected by the deep geochemistry drill-holes only. The Suite footwall altitudes vary from +274.0 to +279.5 m. Thickness varies from 3 to 10 m. It lies over crystalline rocks or their weathering crusts, and over Paleogene Obukhivska Suite sediments. It is overlain by the Neogene limestone sequence and Quaternary sediments. The Suite is composed of quartz, kaolineous, “gluing”, light-grey, greenish-grey, fine-grained to diverse-grained sands. Paleontologically the Suite is not characterized. By analogy with adjacent from the south territory, position in the column and lithology the Suite is ascribed to Badenian regio-stage of Middle Miocene.

Novopetrivskiy regio-stage

Poltavska Series

Novopetrivska Suite (N1np)

Novopetrivska Suite is developed in Berdychivska LTZ, in the far north-eastern part of the map sheet territory, in the small-scale sites preserved from erosion in the dimples of crystalline basement surface. The Suite footwall altitudes vary from +224.8 to +249.5 m. Average thickness is 5-7 m. The Suite lies directly over Precambrian crystalline rocks or their weathering crusts and is overlain by Upper Miocene parti-colored clays or Quaternary sediments. It is composed of sands, rarely secondary kaolines and sand-clayey rocks. The sands are quartz, light-grey, white, slightly kaolineous, fine-medium-grained, regularly-grained, well-sorted. Secondary kaolines are confined to the Suite upper column parts, light-grey to grayish-white, uniform in composition, low-quartz. In places unclear banding is observed caused by various coloring of individual interbeds. Average thickness of secondary kaolines is 3-4 m. Lack of organic remnants, uniform composition, good sorting, fine-graining, kaoline-bearing of the sands suggest for their deposition in shallow- water basin of lake type. Paleontologically the Suite is not characterized; it is extended into adjacent studied map sheet Berdychiv where by the stratigraphic position these sediments are ascribed to Lower-Middle Miocene.

Sarmatian regio-stage

The sediments of Sarmatian regio-stage are developed throughout the map sheet territory except the far north-eastern part (Berdychivska LTZ). By lithology, facial affinity these sediments are clearly divided into three sequences which correspond to the three stages in sedimentation evolution under conditions of paleo-geographic changes over that time (from bottom to top):  sequence of coaliferous sands and clays (N1vp);  sequence of limestones (N1v);  sequence of clays, sands and aleurites (N1gp).

Sequence of coaliferous sands and clays (N1vp)

The Sequence is mainly developed in the basement depressions of intricate shape, with some predomination of sub-longitudinal direction (Fig. 2.7). Normally these sediments lie over basement rocks and their weathering crusts, except the slope of Ukrainian Shield where they are underlain by Paleogene sediments. It is overlain by the sequence of limestones, and in places where the latter is absent – by the sequence of clays, sands and aleurites.

6 Khomora

2 25.4 0 S lu Grytsiv c 7 h 23.1

10 V er bka Lyubar a ilk B ka ych rev De

v Teteri

Biluga

P op ivk Ikopot a Starokostyantyniv

G ra b a rk a

Sluch

6 14.7 I 2 kva 6 0

Do ma kha Stara Synyava 250

B 0 uz 4 ho 44 2 k 1 2

0 0 21.5 0

4 KHMILNYK 2

N o

13 o B s ta 0

vt Kudynka h

si L 5 t 5.2 a u k 2 0 e o

4 S

2 18241 2

46 5

250 4.9 0 2.2 260 1599 5 11.0 1540 14.6 Fosa

Medzhybizh 1 75 9.0 g ou B th

1 0 7

5 2 1580

Letychiv 3.5

0 5 3

vk Vo 1502

0 2.7 0

5 1 2 1 : 500 000 5 kilometers in 1 centimeter km 5 051015 km

10 44 1 2 260 3 21,5 4 5 5

Fig. 2.7. Distribution map of the Sarmatian sequence of coaliferous sands and clays (N1vp) in map sheet M-35-XXII (Starokostyantyniv).

1 – distribution boundaries of the sequence of coaliferous sands and clays; 2 – isopachs; 3 – footwall isohypses; 4 – drill-holes: in numerator – drill-hole number, in denominator – thickness in meters; 5 – probable tectonic breaks.

The Sequence footwall altitudes vary from +216.0 to +277.5 m. The maximum thickness is 39.3 m (Letychiv town area). The lower and upper batches are distinguished in the Sequence. The lower one is preserved from erosion in the deepest sites of paleo-depression and consists of alluvial sediments of the river-course and flood-

47 land facies. The batch is composed of quartz, grey, light-grey, diverse-grained, mainly coarse-grained to gravelous sands with fine weakly-rounded pebble; the sands are often non-sorted and in places at the bottom are slightly cemented by clayey-kaoline material. The sands often alternate with grey, dark-grey, brown clays, diverse-sandy, dense, viscous, non-carbonate. In places, where clays constitute the basal horizon of given batch, they contain clastic material composed of acute and rounded quartz grains. The interbeds of coaliferous, brown- grey to black clays are also observed, often with coalified plant detritus, somewhere with brown coal interbeds from first centimeters to 0.5 m thick. By results of palinological studies of coaliferous clays and brown coal, T.B.Gubkina has determined the spore-pollen spectrum where both spermatophyte and gymnospermous pollen is developed. Spermatophyte mainly include pollen Pinus (Diploxylon and Haploxylori), Picea, Tsuga sp., Nyssa.; gymnospermous pollen – Chenopodiacea, Anacardiacea, Quercus, Betula sp., Fagus sp., Acer sp., Juglans sp., and others. These spectra most likely are similar to the Miocene spore-pollen complexes and do not allow more precise age definition. The upper batch is composed of marine and lagoon-lake sandy-clayey sediments. The sands are mainly quartz, light-grey, clayey in various extents, in places kaolineous, diverse-grained with fine-medium-grained predomination, in the upper batch part commonly calcareous, contain fine fragments of mollusc shells. Somewhere horizontal and wavy parallel, rarely oblique banding is observed. The column of upper batch is described in the quarry nearby Suslivtsi village. In the lower part the batch is composed of quartz, light-grey, fine-grained sands. Visible thickness of this interbed is 0.5 m. Higher in the column is developed quartz, diverse- grained, brownish-yellow, ocherous sand with thin parallel wavy banding. Thickness is 0.5-1.2 m. This sand is further replaced by discontinuous and often pinching interbed of carbonate-quartz sand with numerous mollusc fauna. According to determinations of V.A.Prysyazhnyuk, the major role in the given interbed is played by Ervilia pusilla dissita Eichw., Mactra (Sarmatimactra) eichwaldi crassa Sidor., Donax sp. ind., and others, indicating Early Sarmatian age of sediments. By results of granulometric analysis, in fine-grained sands the fraction 0.1-0.25 mm predominates constituting 83-86.6% of the rock volume. The clayey fraction (0.001-0.01 mm) constitutes 4.14-4.28%. In all samples the light fraction in mainly composed of quartz in amounts from 85 to 100%. Hydromica- clayey minerals are contained in the fine-disperse fractions where their amount attains 50-75%. The heavy fraction of all sands is more or less uniform in composition containing ilmenite, leucoxene, rutile, staurolite, zircon, tourmaline, garnet. The clays are rarely observed. They are mainly grey, dark-grey, in places sandy and aleuritic up to clayey aleurites, often calcareous, dense, contain mollusc imprints and shells. In places they constitute interbeds up to 8.7 m thick. In the clays V.A.Prysyazhnyuk had determined molluscs Venerupis (Polititapes) sp. ind., Musculus sarmaticus Gat., Cerastoderma (Obsoletiforma) ex gr. gatyevi Koles, and others, characteristic for Sarmatian regio-stage.

Sequence of limestones (N1v)

The Sequence is developed in the western and south-western parts of the map sheet, except the sites of modern erosion in the valleys of major rivers (Fig. 2.8). A number of Sarmatian limestone exposures at the surface are mainly confined to the slopes of major river valleys: South Boug, Buzhok, Sluch, Ikva, Khomora, and others. The Sequence is underlain by the sequence of coaliferous sands and clays, and in places where the latter are absent in the western map sheet part – by Paleogene Obukhivska and Kyivska suites. Outside the distribution areas of mentioned stratons the Sequence lies over the rocks of crystalline basement and their weathering crusts. It is overlain by the sequence of clays, sands and aleurites and Quaternary sediments. The Sequence is mainly composed of limestones with single thin marl interbeds. Rarely carbonate- quartz sand and sandstone interbeds are observed, as well as thin clay interbeds occurring in limestones. The Sequence footwall altitudes vary from +229.4 to +296.9 m. The maximum thickness is 31.0 m (Shcherbani village area). Limestones are mainly detritic-oolitic, detritic-pelitomorphic, rarely detritic and fine-oolitic, yellowish- light-grey, brown in the upper parts, black, manganese-enriched at the bottom, somewhere fractured, often with minor cavernous hollows, with diverse-grained quartz sand admixture. Detritic and detritic-pelitomorphic limestones consist of the fragments and solid mollusc shells, rarely foraminifera, cemented by fine-crystalline carbonate. These limestones are mainly confined to the upper column parts. Oolitic limestones in places by 90- 95% consist of rounded oolites 1-5 mm in diameter with concentric-shell structure. Oolite core is mainly composed of quartz grains, rarely fine shells and crypto-crystalline calcite. The outer part is composed of

48 concentric pelitomorphic carbonate layers superimposed one onto another. These limestones are cemented by fine-grained carbonate and observed at the Sequence bottom. Most widespread are detritic-oolite and oolite- detritic limestone varieties composed of the fragments and solid mollusc shells and oolitic material.

4 6 0 1

2.8 Khomora 2.9

4 S 0 5 l 2 2 7 u Grytsiv c 2.0 h

5.1 2.1

2 6

0 V er bka 3 Lyubar a ilk

6.9 B 2 0 a

5 chk 5 y

0 rev 2 De

14114

0 3 2 2.7 14029 2.0 14036

Teteri 2 5 0 3.0

Biluga 14206

124 5 0 5

4.5 2 14174

2 6.5 4 0 5 3.0 0

250 14226 Po 12.0 piv 11 ka Ikopot 4.7

Starokostyantyniv

260 14310

8 2 6 0 G 10 ra 3.0 4.7 9 b a rk 6.0 8.7 14264 14269 a 16.0 12.5 h Sluc 14194 14251 15.0 11.3

27 1 14261 14267

5 0 0

17.0 21.5 14141

14272 12.02

18225 10 12.0 0

18.5 0 6 19 2 30 12.2 18226 3.0 D

17.2 om

akh 10 a Ikva

171 Stara Synyava 240 11.7 0

270 6 2 4 250 2 0 45 1573 12.8 250 12.6 KHMILNYK Bu 17 zh 44 ok 8.9 12 24.0

0 9.7 4 1600

118 g 5 2557 25 18.0 u

N o ov 17.9 os B 0.8 Kudynka 2 tav ts h

6 i L t

0 ake 2 u

o 1543 6 S

25 46 0 0 0 1 1546 14.8 6.8 1555 1550 12.9

15.0 14.9 2

5 1552 0 1558 16.0 4.0 1549 116 Medzhybizh 14.1 Fosa 1.8 18245

2 g u 0

6 Bo 10.0

0 th

ou 2

0 S

1 14

1 15 2 0 1583

4.0 0 8 0 1506 2.3 0 17.0 26 7 2 0.4 Letychiv 114 90 vk 0 2 Vo 1504 6

18238 14.1 80 1505 2

1594 2 70 1502 11.5 1 2 1 15.0 129 5.0 0 10.0 11.0 5 2.4

1 : 500 000 5 kilometers in 1 centimeter km 5 0510 15 km

10 4 1 5 2 260 3 2.0 4 5

Fig. 2.8. Distribution map of the Sarmatian sequence of limestones (N1v) in map sheet M-35-XXII (Starokostyantyniv).

1 – distribution boundaries of limestones; 2 – isopachs; 3 – footwall isohypses; 4 – drill-holes: in numerator – drill-hole number, in denominator – thickness of sediments in meters; 5 – probable tectonic breaks.

Quartz-carbonate and carbonate-quartz sands and sandstones are often observed but quite locally. They are mainly light-grey, rarely brownish-yellow. The rocks are composed of the fine fragments of mollusc shells

49 and diverse-grained, mainly coarse-grained, weakly-rounded quartz sand; they are confined to the bottom part of limestone sequence. Thickness of interbeds normally does not exceed 1.0-1.5 m. By results of mineralogical analysis, quartz-carbonate sand contains ilmenite, garnet and zircon. The marls are very rarely observed and are developed both in the lower and upper column parts. In the marls V.A.Prysyazhnyuk had determined unique complex of the land molluscs. For the first time in the Middle Sarmatian abundant development is noted for Stribilopsides Stribilops exgr. ukrainica Steki, Stribilops sp. nov., Stribilops ex gr. tiarula (Papl.), Stribilops sp. ind.), characteristic for Lower Sarmatian, as well as predominating position in gastropoda for the representatives of Albinula (Gastrocopta gracilidens Sandb., G. acuminata Lartetti Dup., G. steklovi Prus., and others). The clays, like marls, are quite rarely observed and are known in the area of Chaplya village. They are developed in thin lens-like interbeds in limestones. The clays are brownish-grey, in places up to dark-grey, often coaliferous. Development of the Sequence is related to the coastal-marine environments. Slight sea level changes had led to the formation of desalinated lagoons, in places up to swamping (coaliferous clays, coalified fossil detritus). These events were short-term (low thickness of clay and marl interbeds) and connection with marine basin was quickly restored. L.F.Goncharuk in the organogenic limestone has determined Middle Sarmatian fauna: Triloculina moinornata Didk., Quinqueloculina consobrinaplana Volosh., Q. badenersis Orb., Elphidium reginum (Orb.).

Sequence of clays, sands and aleurites (N1gp)

This Sequence in developed almost everywhere in Khmelnytska LTZ and in the far western part of Berdychivska LTZ, except erosion sites in the valleys of major rivers. The Sequence exposures at the surface are noted in many quarries and outcrops. It lies mainly over the sequence of limestones, and in places where the latter is absent – over the sequence of coaliferous sands and clays, in places over Buchatski sediments of Khmilnytska paleo-depression and over crystalline rocks and their weathering crusts. Over most part of the area the Sequence is overlain by Quaternary sediments. In the north- eastern part of the territory in Berdychivska LTZ it is overlain by the sequence of parti-colored clays. The Sequence footwall altitudes vary from +210.0 to +300.0 m. The maximum thickness is 86.5 m (to the north of Parkhomivtsi village). The rock lithology of the Sequence is quite variable. It consists of clays, aleurites and sands with thin lens-like limestone interbeds. Conventionally the Sequence is divided in two batches. The lower one comprises thin intercalation of grey and dark-grey aleuritic clays and aleurites, rarely sands with micro-fauna. The clays in this column part are grey, dark-grey, dense, argillite-like, in places contain coalified plant remnants. Aleurites are also grey and dark- grey, mica, clayey, dense. Sand interbeds are scarce. The sands are mica-quartz, fine-micro-grained, clayey. Upward in the batch the sands alternate with grey, greenish-grey clay and aleurite interbeds. The upper batch is mixed in composition. The clays are mainly light-grey, greenish-grey, ocher-brown in the interbeds, spotty, with ocher-brown spots, at the top often ocherous, iron-enriched by the bedding planes, sandy in various extents, scraggy, mainly aleuritic, carbonate, somewhere viscous, lumpy. In places, where clays lie directly above weathering crusts, they often contain considerable amount of acute quartz fragments up to gravel in size. Aleurites of the upper batch are light-grey, ocherous-brown in interbeds, quite variable in color, clayey, with gradual transitions into aleuritic clays and micro-grained sands. The sands of upper batch are quartz, mica-quartz, yellowish-light-grey, greenish-grey, clayey, mainly horizontally-banded. In places the sands are enriched in coaliferous matter. They are noted over entire batch column, their thickness attains 27.2 m. In the granulometric composition of the sands the fractions 0.1-0.25 and 0.25-0.5 mm predominate. The major mineral in light fraction is quartz. The heavy fraction minerals include ilmenite, garnet, zircon, rarely leucoxene, rutile, tourmaline. In the south-western part of the map sheet in the middle column part the lens-like interbeds of yellowish-light-grey, grey, detritic-oolite limestones are observed. Most often they are noted in the area of Bokhna village. Thickness varies in the range 3-6 m. The maximum thickness of 10.0 m is noted to the north- west from Bokhna village. According to determinations of T.B.Gubkina, the spore-pollen complex in the Sequence is weakly preserved and contaminated. Gymnospermous pollen Pinus Diploxylon and Haploxylori, Picea, Taxodiaceae, Carya sp. predominate. Of spermatophyte the pollen Betula sp., Quercus, Ericaceae, Chenopodiaceae are noted. Association of above forms is characteristic for Late Miocene spore-pollen complex. Fauna findings in these sediments exhibit rich complex of marine, fresh-water and surface molluscs which correspond to Middle

50 Sarmatian. Of the most developed molluscs, according to V.A.Prysyazhnyuk, are as follows: Mactra podolica Eichw., Mactra sp. ind., Cerastoderma (Plicatiforma) ex gr. fittoni Orb., Venerupis (Polititapes) vitalianus Orb., and others. Fresh-water molluscs include Valvata ex gr. piscinalis Mull., Bithynia sp. ind., Planorbarius sp. ind., Lymnaea ex gr. spirorbis Linn., and others. The surface molluscs mainly include Carychium schlickumi Prys., Gastrocopta nouletiana sp., and others. After nano-plankton studies, S.A.Lyulyeva has determined widespread Coccolitus pelagicus (Wall.), Reticulofenestra pseudoumbilica (Garth.), Helicosphaera carteri (Wall.), and others, characteristic for Sarmatian sediments. In the clays of this Sequence, which lie directly over the sequence of limestones, thin interbed of clot- foraminifera limestone is encountered with sulphide admixture, fish bones, where in addition to the mollusc shell detritus foraminifera are determined (V.Ya.Didkovskiy): Quinqueloculina consobrina Orb., Q. prava Didk., Q. ex gr. conforma Orb., Nonion bogdanowiszi Vol., Elphidium masselum Orb., E. hauerinum Orb. By age these forms are transitional from Early to Middle Sarmatian. Thus, it can be concluded that development of the sequence of clays, sands and aleurites had commenced at the boundary of Early and Middle Sarmatian (in the north-western part of the area) and continued over Middle and probably Late Sarmatian time (in the central and eastern parts), that is, both the lower and upper boundaries are relocating.

Sequence of parti-colored clays (N1sg)

The sequence of parti-colored clays is developed in the north-eastern part of the area (Berdychivska LTZ), where it is preserved from erosion at the uplifted watersheds. The Sequence lies over Novopetrivska Suite and crystalline rocks and their weathering crusts, and in the eastern part of Khmilnytska LTZ – over Sarmatian sequence of clays, sands and aleurites; the Sequence is overlain by the sequence of red-brown clays, and in places where the latter is absent – by Quaternary sediments. The Sequence footwall altitudes vary from +255.3 to 277.5 m. The maximum thickness of parti-colored clays is 44.1 m (to the east of Lysogirka village). The Sequence is composed of parti-colored, spotty, heavy, dense, mainly non-carbonate or slightly- carbonate, actually non-banded, often with sliding surfaces, greasy in touch clays. Parti-coloring is expressed in the ocherous, brownish-yellow, cherry-red, raspberry, brownish-dark-grey spots on the background of common greenish-grey and light-grey rocks. Often the clays contain friable light-grey to white carbonate concretions from 1-2 mm to 1-2 cm in size, arranged in aggregates, as well as ironiferous and manganese patterns 1-2 mm in size. The sands are rarely observed in thin (up to 4.5 m) interbeds. They are quartz, grey, greenish-grey, spotty-ocherous, fine-micro-grained, in places medium-grained, clayey, somewhere with unclear-expressed horizontal banding. Aleurites are also developed in subordinate amounts and observed in thin interbeds. Aleurites are mica- quartz, greenish-grey, clayey, spotty-ocherous, in places horizontally-banded. By the results of granulometric analysis, in parti-colored clays the fractions 0.01-0.05 mm and 0.001- 0.01 mm predominate. In the coarse fraction (>0.05 mm) quartz predominate with minor feldspar and hydromica-clayey aggregates. Of the heavy fraction minerals the iron hydroxides, pyrite, ilmenite, leucoxene and rutile are noted. Almost all samples contain minor amounts of zircon, kyanite, tourmaline, garnet, staurolite. Parti-colored clays differ from the clayey sediments of Sarmatian sequence of clays, sands and aleurites in almost complete lacking of banding and much higher spotty patterns, often with cherry, red, raspberry spots. The rocks were developing in the sub-aqueous continental environments. The Sequence does not contain any fauna. The spore-pollen complex is poor. Single Miocene examples include pine-tree (Pinus Diploxylon and Haploxylori), fir (Picea, Myricacea), beech (Fagus sp.), oak (Quercus). The Late Miocene age of the Sequence is defined by its stratigraphic position.

101Pliocene division

Sequence of red-brown clays (N2čb)

In the studied area red-brown clays comprise the youngest pre-Quaternary sediments. They are confined to the elevated sites of ancient plateau and developed in the eastern part of the studied area. In the modern relief the sites of their development coincide with the flattened watersheds. In Berdychivska LTZ the Sequence lies over parti-colored clays, and in the south-eastern part of Khmelnytska LTZ – over the sequence of clays, sands and aleurites. The surface exposures are noted in the minor quarries in the area of Rozhny and Ivky villages. The red-brown clays are overlain by Eo-Pleistocene and Lower Neo-Pleistocene rocks.

51 The footwall altitudes of red-brown clays vary from +265.9 to +340.6 m. The maximum thickness is 26.0 m (to the south-west from Podolyany village). The Sequence is mainly composed of brownish-grey clays, mainly with reddish and brownish shade, in places with red-brown spots up to first centimeters in size, scraggy, dense, glued, with rugged surface, often sandy. The sand enrichment is especially characteristic for the lower part of the Sequence where the clays are replaced by the clayey sand. In the clays the iron-manganese spots and carbonate concretions are observed. Thin (up to 2.0 m) interbeds of fine-grained quartz sands and aleurites in the clays are subordinate. Their color is from light-grey to bright-pink and brown, often with numerous brown spots. The thin sub-horizontal banding is also noted. The spore-pollen complex of red-brown clays is very poor and includes pollen of pine-tree (Pinus) oak (Quercus) and heathers (Ericaceae).

60Quaternary System

According to the zonation scheme of Quaternary sediments in Ukraine [18], the map sheet territory is located is the loess region of Ukrainian platform plain, in two sub-regions – Northern peri-glacial and Central- Ukrainian. The Quaternary cover exhibits diverse genetic types and discontinuous thickness depending on sedimentation conditions in Quaternary time in different morpho-structures. Comparison of Quaternary sediments structure, their thickness, hypsometric position, influence of neo-tectonic motions made possible to distinguish three areas in the Northern peri-glacial sub-region of the map sheet territory – Lyubarskiy C-II-3-a, Khomorsko-Teterivskiy C-II-3-b (subdivided into Ikopotskiy, Sluch-Khomorskiy, Sluch-Teterivskiy sub-areas), Khmilnytskiy C-II-3-c; in the Central-Ukrainain sub-region three areas are distinguished – Khmelnytskiy C-II-5- a (includes Khmelnytskiy and Trebukhivskiy sub-areas), Litynskiy C-II-5-b, and Letychivskiy C-II-5-c. The Quaternary sediments do cover the older rocks with almost solid blanket and are lacking only in places of pre-Quaternary rock exposures along the river valleys and on the steep gully and ravine slopes. Their thickness is not persistent and varies from 1-2 to 38-40 m. Most complete columns are preserved on the watershed plateau of Litynskiy area in between South Boug and Ikva rivers. At the surface are mainly exposed the sediments of Neo-Pleistocene upper section. The middle section sediments are mapped in the north-east of the map sheet in Lyubarskiy area and in the local sites of the territory (the area of Parkhomivtsi, Grushkivtsi, Novoselytsya, Lagodyntsi, Lysogirka, Suslivka villages). The surface exposures of the Neo-Pleistocene lower section rocks are noted in some outcrops (nearby Biletske, Kudynka villages), whereas Eo-Pleistocene sediments are only intersected by drill-holes. Quaternary sediments commonly overlie Neogene rocks – Upper Miocene clays, sands and limestones, rarely red-brown and parti-colored clays, and somewhere – the rocks of crystalline basement and their weathering crusts. In the western part of map sheet, in the valleys of South Boug and Buzhok rivers, at small sites they lie over Paleogene rocks.

102Pleistocene division

According to the Stratigraphic Code of Ukraine, the Pleistocene division includes Eo-Pleistocene and Neo-Pleistocene sections.

Eo-Pleistocene section

This one includes sediments of the lower and upper branches. The rocks are mainly developed at the watersheds and also are preserved from erosion in Khmilnytsko-Lukashivska transition valley (Podolyany village). The sediments are intersected by drill-holes.

Lower branch

Berezanskiy climatolith. Aeolian-deluvial sediments /vdE1br/ are locally developed at the watersheds of South Boug and Ikva rivers. They lie over the sequence of red-brown clays and often are connected with the latter by gradual transitions. The footwall altitudes vary from +283.5 (Podolyany village) to +303.6 m (Rozhny village). The rocks include bluish-brown, brown-yellow, bluish-grey clays, in places with ocherous spots, rarely with carbonate concretions. Thickness of sediments is up to 0.9 m.

Upper branch

Upper Eo-Pleistocene branch includes mainly sub-aerial facies sediments of warm and cold sedimentation phases. Kryzhanivskiy climatolith. Eluvial-deluvial sediments /edEIIkr/ are developed at the elevated watersheds in Lithynskiy area and also in Khmilnytsko-Lukashivska transition valley (Podolyany village). Kryzhanivski soils lie over Miocene clays, sands and limestones, Pliocene red-brown clays, rarely parti-colored clays, and also over aeolian-deluvial sediments of Berezanskiy climatolith. The footwall altitudes vary from +284.3 (Podolyany village) to 313.4 m (Chaplya village). The rocks include clays and heavy loams with characteristic red coloring – red-brown, in places ocherous due to iron enrichment and limonitization, in places with manganese spots, often sandy, with flint- carbonate concretions. Thickness of sediments is up to 1.9 m. By granulometric composition these are mainly (more than 90%) fine-disperse clays with particle size 0.001-0.01 mm. Illichivskiy climatolith. Aeolian-deluvial sediments /vdEIIil/ are least developed of the Eo-Pleistocene sediments. They are preserved at the elevated sites of Litynskiy area where they are intersected by single drill- holes in the area of Rozhny and Ilyatka villages, and in Khmilnytsko-Lukashivska transition valley nearby Podolyany village. They lie over Kryzhanivskiy climatolith and from the latter sediments differ in the lighter coloring and less carbonate content. The footwall altitudes vary from +285.2 (Podolyany village) to +306.4 m (Rozhny village). The rocks include heavy loams and light-brown spotty clays from 0.4 to 1.4 m thick.

Eo-Pleistocene – Neo-Pleistocene sections

Eo-Pleistocene section – lower branch of Neo-Pleistocene section

Aeolian-deluvial and eluvial sediments /vd,eE-PI/ are distinguished in the eastern part of Litynskiy area. They lie over Neogene sands and clays and are overlain by the soils of Zavadivskiy climatolith. The sediments include yellow-brown, dark-brown, medium and heavy loams, from 4.0 to 7.0 m thick.

Neo-Pleistocene section

The Neo-Pleistocene sediments are developed almost everywhere in the studied map sheet.

Lower branch

In the studied area the rocks of all climatoliths of the lower Neo-Pleistocene branch are developed. They are intersected by most drill-holes at the watersheds and on their slopes. The surface exposures are observed along the river valleys and on the gully slopes. Shyrokynskiy climatolith. Eluvial-deluvial sediments /edPIsh/ are developed in Litynskiy area where they are intersected by many drill-holes, and also in Khmilnytsko-Lukashivska transition valley (Podolyany village) and in the east of Trebukhivskiy sub-area (Grushkivtsi village). The surface exposures are observed in the outcrops nearby Biletske and Kudynka villages. They lie over Upper Eo-Pleistocene (Kryzhanivski and Illichivski) sediments, in places over Pliocene sequence of red-brown clays, and are overlain by the loess-like loams of Pryazovskiy, Tyligulskiy and Sulskiy climatoliths. The footwall altitudes vary from +300.0 (Ilyatka village) to 335.0 m (Grushkivtsi village). The rocks include meadow, meadow-loess and meadow-swamp soils – brown-grey, dark-brown, brown, yellow-brown clays and heavy loams, often with bluish and ocherous spots, in places with ironiferous and manganese spots, often with sand material admixture. Thickness of sediments varies from 0.4 to 2.7 m. From the soil of Kryzhanivskiy climatolith they differ in parti-coloring (bluish spots) and lack of red shade. Pryazovskiy climatolith. Aeolian-deluvial sediments /vdPIpr/ are locally developed, mainly at the elevated sites of Litynskiy area, in the east of Trebukhivskiy sub-area. The rocks lie over sediments of Shyrokynskiy climatolith and are overlain by Martonoski soils. The footwall altitudes vary from +300.4 m (Ilyatka village) to +336.0 m (Grushkivtsi village). The rocks include loess-like, pale-grey, light-pale, light-grey, light-brown, medium to heavy, dense loams, in places with sand admixture, rarely with carbonate concretions. Thickness varies from 0.5 to 3.0 m. Budatskiy ledge. Alluvial sediments /aPIbk/ of this ledge are intersected by a drill-hole in Letychivska transitional zone (DH 1530, Dyakivtsi village) [51]. They lie over the surface of Sarmatian clays and are overlain

53 by sub-aqueous rocks of Martonoskiy climatolith. The rocks are distinguished by their position in the column. The footwall altitude is +291.5 m, thickness – 3.5 m. It is possible that these are terrace sediments of Pra-Boug river or one of its branches. The rocks include quartz, yellow-grey to brown, diverse-grained, mainly fine-medium-grained sands. Martonoskiy climatolith. Eluvial-deluvial sediments /edPImr/ are developed in Litynskiy area, Trebukhivskiy sub-area (in the eastern part) and Letychivska transitional zone. They lie over Shyrokynski soils and are overlain by Sulski and Tyligulski loess-like loams and Lubenski soils. Thickness varies from 0.5 m (Ilyatka village) to 3.9 m (Chaplya village). Sub-aerial facies include meadow and meadow-forest glued soils – brown, light-brown, brown-grey, often yellowish, in places with brownish and reddish shades, heavy loams, rarely – dense, mainly non-carbonate clays, in places with sand admixture. Sub-aqueous facies are genetically linked with alluvial sediments of Budatskiy ledge. These include flood-land-swamp clayey soils, mainly brown, with ocherous spots, sandy. The sediments of Martonoskiy climatolith differ from Shyrokynski soils in the yellowish coloring. Sulskiy climatolith. Aeolian-deluvial sediments /vdPIsl/ are only developed at the watersheds of Litynskiy area and in Letychivska transitional valley. They are intersected by drill-holes while the surface exposure is only known in the outcrop nearby Biletske village. They lie over the soils of Martonoskiy climatolith and are overlain bu Lubenski soils. The footwall altitudes vary from +285.6 (Podolyany village) to +339.5 m (Yaroslavka village), thickness varies from 0.3 m (Ilyatka village) to 5.5 m (Chaplya village). The rocks include pale-brown-grey, grayish-pale, yellow-pale, mainly medium loams, in places sandy, somewhere with fine carbonate concretions. From the loams of Pryazovskiy climatolith they differ in the pale shade, they are less dense and lighter. Lubenskiy climatolith. Eluvial-deluvial sediments /edPIlb/ in Litynskiy area are developed almost everywhere but occupy limited fields in Trebukhivskiy sub-area and in Letychivska transitional valley. The only surface exposure is encountered in the outcrop nearby Biletske village. The rocks lie over the sediments of Sulskiy or Martonoskiy climatoliths, rarely over Pliocene red-brown clays, and are overlain by Tyligulski loams, in places by the Middle Neo-Pleistocene Zavadivski soils or the sediments of Dniprovskiy climatolith. The footwall altitudes vary from +269.9 m (Yaroslavka village) to +346.3 m (Parkhomivtsi village). The rocks include forest, meadow-forest and meadow soils, brown-grey, grey, heavy-loamy, dense, hydromorphic, in places with ocherous iron-enrichment and manganese spots. Thickness varies from 0.5 to 3.5 m. From the older soils they differ in the grey coloring and complete lacking of clays. Tyligulskiy climatolith. Aeolian-deluvial sediments /vdPItl/ are locally developed at the watersheds of Litynskiy area. The only surface exposure is known in the outcrop nearby Biletske village. In Letychivska transitional valley they are intersected by DH 1530 nearby Dyakivtsi village [51]. The rocks lie over the soils of Lubenskiy climatolith and are overlain by the sediments of Zavadivskiy climatolith. The footwall altitudes vary from +270.4 m (Yaroslavka village) to +342.0 m (Grushkivtsi village). Thickness varies from 0.2 to 16.9 m (Yaroslavka village). The sediments include pale-yellow, brown-grey, grayish-yellow, light-grey, light and medium, loess- like, dense, thin-platy, carbonate loams, often with fine carbonate concretions and sand material admixture. From the loess-like loams of Sulskiy and Dniprovskiy climatoliths they differ in the yellow coloring. They also have less specific weight than the loams of Sulskiy climatolith.

Lower-middle branches

Sub-aqueous facies of the lower-middle Neo-Pleistocene branches include undivided sediments of Krukenytskiy and Khadzhybeyskiy ledges of the 5-6th over-flood terrace, and sub-aerial facies – eluvial and aeolian-deluvial sediments of Shyrokynskiy-Zavadivskiy climatoliths. th Krukenytskiy-Khadzhybeyskiy ledges undivided. Alluvial sediments of the 5-6 over-flood terrace /aPI- IIkn-hd/ are developed in the valleys of South Boug, Buzhok, Ikva rivers where they constitute the lower column parts of terrace sediments. They are intersected by drill-holes and are known in some outcrops in the valleys of South Boug and Ikva rivers. In the South Boug river valley they are lacking at the sites where terrace socle is composed of Sarmatian limestones – in the left bank from Stavnytsya village to Markivtsi village, and in the right bank – to the south from Trebukhivtsi village and from Letychiv town to Novokostyantyniv village. In between Shchedrova and Kudynka villages the rocks are developed in the fragments, and in between Novokostyantyniv and Svichna villages they are lacking at all in the both valley banks. Alluvial sediments lie over the rocks of crystalline basement and their weathering crust or over Sarmatian clays, sands and limestones, and to the south-west from Medzhybizh town – over Paleogene sandy sediments. They are overlain by the eluvial-deluvial soils of Kaydatskiy and Vytachivskiy climatoliths, as well

54 as aeolian-deluvial sediments of Buzkiy-Prychornomorskiy climatoliths. At the sites, where denudation processes predominate (Lysogirka village area), they are overlain by deluvial-aeolian and eluvial sediments of Kaydatskiy-Prychornomorskiy climatoliths – sands, sandy loams, rarely loams. The footwall altitudes vary from +268.0 m (Mytkivtsi village) to +283.4 m (Ivankivsti village). The minimum thickness is 1.5 m (Kopachivka village), and the maximum one – 4.0 m (Mytkivtsi village). The rocks include grey, yellow-grey, quartz and feldspar-quartz sands with brown-ocherous clayey interbeds, in places with brown-yellow sandy loam interbeds. Somewhere in the lower column part the sands contain pebble and gravel of quartz, limestone, crystalline rocks, and “Carpathian pebble”. The first information of fauna findings in terrace sediments were provided by V.D.Laskarev (1914), and then by V.G.Bondarchuk (1931). P.F.Gozhyk in 1969 [15] at the outskirt of Medzhybizh town, in alluvium of the 5-6th over-flood terrace, had determined molluscs: Viviparus diluvianus crassus, V.bugensis, Lithoglyphus neumayri, Theodoxus serratiliformis, and others, as well as fine mammals: Sorex praearaneus Kormos, Sorex Sp., Microtus gregalis Pall., M.ex gr. ratticepoides Hint., Microtinae gen?, and others. After results of these studies, the age of the 5-6th over-flood terrace of South Boug river was defined ass Likhvinskiy (scheme of the Stratigraphic Committee of USSR, 1964), or Mindelryskiy (by Alpine scale). In addition, in these sediments the signs of the material culture of ancient man are found [7]. In the heavy fraction of alluvial sands increased content of ilmenite and leucoxene is determined – 13.4 km/m3, rutile and anatase – 0.19 kg/m3, as well as single signs of pyrope, chalcopyrite, topaz. Shyrokynskiy-Zavadivskiy climatoliths. Eluvial and aeolian-deluvial sediments /e,vdPI-IIsh-zv/ are mapped in Trebukhivskiy sub-area, to the west of Grushkivtsi village. Due to the low thickness (from 0.7 to 3.0 m) of established climatolith these units are indicated as the single complex. Their distribution boundary almost coincides with the contour of minor neo-tectonic uplift distinguished on the results of satellite image processing. The footwall altitude is 335.0 m, total thickness – 11.0 m. Lithology of sediments is given in the description of individual climatoliths.

Middle branch

Middle Neo-Pleistocene branch in the studied area includes various genetic types of sediments in Zavadivskiy, Dniprovskiy, Kaydatskiy and Tyasminskiy climatoliths. They are developed almost everywhere and intersected by most drill-holes. The natural surface exposures are known along the river valleys and at the watershed relief parts. By the square, eluvial-deluvial sediments of Zavadivskiy and Kaydatskiy climatoliths are most widely developed. Sub-aqueous facies mainly include alluvial-fluvio-glacial, water-glacial and lake-glacial sediments of Dniprovskiy climatolith. Zavadivskiy climatolith. Eluvial-deluvial sediments /edPIIzv/ are developed in Litynskiy area almost at all watersheds and on their slopes, being absent in the river valleys and deep gullies. They are completely lacking in the Northern peri-glacial region where they were eroded in Dniprovskiy time. In transitional valleys the soils of Zavadivskiy climatolith are also eroded and only preserved in the minor remnant in Letychivska transitional valley (Dyakivtsi village). To the west from Grushkivtsi village the soils are exposed at the surface. The sediments lie over loess-like loams of Tyligulskiy climatolith and Lubenski soils, and actually always are overlain by the sediments of Dniprovskiy climatolith. The footwall altitudes vary from +267.5 m (Chaplya village) to +348.0 m (Parkhomivtsi village). Thickness varies from 0.5 to 3.8 m. Of the all sediments of warm phases Zavadivski soils are thickest and often consist of several sub- horizons. These are meadow-forest and forest soils, brown, grayish-brown, rarely ocherous-brown, in places with red and brown shade, heavy-loamy. The lower sub-horizon is darker and includes mainly brown forest soils with iron-manganese beans. The upper sub-horizons are lighter – red-light-brown. Hydromorphic soils are intersected by drill-holes in the area of Yablunivka and Grechyntsi villages. They comprise swamp, meadow-swamp, brown-ocherous, yellow-brown, rarely brown-grey, banded, medium- heavy-loamy soil sediments. Zavadivski soils differ from Lubenski ones in prevailing brown and red coloring, and lack of humus horizon. Dniprovskiy climatolith. In the studied map sheet it includes three genetic types: aeolian-deluvial, water-glacial and lake-glacial, alluvial-fluvio-glacial. Aeolian-deluvial sediments /vdPIIdn/ are widely developed in Litynskiy area and western part of Trebukhivskiy sub-area. At the watersheds they lie over Zavadivski soils, and on the slopes – over Lower Quaternary sediments. The footwall altitudes vary from +275.9 m (Dashkivtsi village) to +348.8 m (Parkhomivtsi village). These are loess-like pale-yellow, rarely light-grey, light and medium, dusty, calcareous loams, often with carbonate concretions up to first centimeters in size. Thickness varies from 0.7 m on the slopes to 16.0 m at

55 watersheds. From the older loess-like loams they differ in the lighter coloring and less specific weight. These rocks comprise distinct marker horizon within the loess-like rocks. Alluvial-fluvio-glacial sediments /afPIIdn/ are developed in Letychivska and Khmilnytsko-Lukashivska transitional valleys. They lie over eroded surface of Sarmatian clays, sands and limestones, rarely on Eo- Pleistocene and Lower Neo-Pleistocene sediments preserved from erosion. The rocks are overlain by the soil sediments of Kaydatskiy-Vytachivskiy climatoliths or the rocks of Buzkiy-Prychornomorskiy climatoliths: deluvial-aeolian and eluvial or aeolian-deluvial and eluvial. The footwall altitudes vary from +251.0 to +303.0 m. The rocks include grey, yellow-grey, brown-yellow, quartz, in places with minor feldspar and mica, diverse-grained sands, at the bottom often with fine gravel and pebble, somewhere with sandy loam and loam interbeds. The sand is weakly-sorted, rounded in various extents, clayey, in places ocherous. Somewhere intercalation of interbeds with different grain size is observed. Thickness varies from 0.9 to 25.9 m (to the east from Dyakivtsi village). Water-glacial and lake-glacial sediments /f,lgPIIdn/ are developed almost everywhere in the Northern peri-glacial region where they lie at the bottom of Quaternary column. At the watershed they are overlain by the soils of Kaydatskiy-Vytachivskiy climatoliths and loess-like loams of Buzkiy-Prychornomorskiy climatoliths. In the river valleys these sediments somewhere are exposed at the surface. The footwall altitudes vary from +256.3 to +298.0 m. The rocks include yellow-grey, grey, quartz, clayey, often banded sands, containing lenses and interbeds of coarse-grained non-sorted sands or greenish-grey loams, sandy loams, rarely sandy clays. In places loams and sandy loams predominate. Thickness of sediments varies from 1.1 to 17.3 m. In DH 1529 nearby Litynka village the lake aleurites is intersected where the surface and fresh-water cold-loving molluscs are determined [50]. Kaydatskiy climatolith. Eluvial-deluvial sediments /edPIIkd/ are developed almost everywhere, both at the watersheds and slopes, and also in the transitional valleys; they are intersected by most drill-holes, and the surface exposures are noted in many outcrops. The rocks lie over loess-like Dniprovski loams, rarely older sediments (mainly on the slopes), and in transitional valleys – over sub-aqueous facies of Dniprovskiy climatolith. In the Northern peri-glacial sub-region they overlie water-glacial and lake-glacial sediments. The rocks are overlain by Prylutski soils, rarely loams of Tyasmynskiy climatolith. The rocks comprise light-grey to brown with various shades loess soils, medium- and light-loamy, rarely heavy-loamy, dusty, irregularly dense. Their thickness varies from 0.5 to 3.7 m, being 1.3-2.4 m in average. In the transitional valleys the soils of Kaydatskiy climatolith are mainly hydro-morphic, aqueous, rarely meadow, black-earth-meadow, glued, heavier (medium- and heavy-loamy), in places sandy loamy, banded, with manganese spots. The brown shades predominate and ocherous spots are observed somewhere. The rocks are mapped within the single complex of eluvial-deluvial sediments of Kaydatskiy- Vytachivskiy climatoliths /edPII-IIIkd-vt/. Tyasmynskiy climatolith. Aeolian-deluvial sediments /vdPIIts/ are locally developed in Litynskiy area and in Letychivska transitional valley. They are intersected by some drill-holes and their surface exposures are noted in the outcrops nearby Chekhy and Ivky villages. The rocks lie over Kaydatski soils and are overlain by Prylutski soils. The footwall altitudes vary from +271.7 (Chekhy village) to +328.6 m (Chaplya village). These are thin (less than 0.4 m) interbeds of pale, yellow-pale, yellow-brown, light and medium, in places loess-like loams, mainly slightly calcareous, in places sandy. The rocks are mapped within the single complex of eluvial-deluvial sediments of Kaydatskiy- Vytachivskiy climatoliths /edPII-IIIkd-vt/.

Middle-upper branches

Sub-aqueous facies of Middle-Upper Neo-Pleistocene branches include alluvial sediments of undivided Cherkasko-Trubizka over-flood terrace, and in sub-aerial facies eluvial-deluvial rocks of Kaydatskiy- Vytachivskiy climatoliths are distinguished. In addition, in 5-6th over-flood terrace the undivided deluvial- aeolian and eluvial sediments of Kaydatskiy-Prychornomorskiy climatoliths are distinguished. Cherkaskiy-Trubizkiy ledges. Undivided alluvial sediments /aPII-IIIčr-tb/ are preserved at some places along major rivers (South Boug, Buzhok, Ikva, Sluch). The rocks are intersected by drill-holes and are known in some outcrops. They lie over the rocks of crystalline basement and their weathering crust, Sarmatian clays, sands and limestones, and over eroded surface of alluvial sediments of 5-6th over-flood terrace. In the area of Golovchyntsi village they are underlain by Paleogene sands and sandstones, and overlain by mainly undivided

56 deluvial-aeolian and eluvial sediments of Vytachivskiy-Prychornomorskiy climatoliths, much rarely – Vytachivski soils and aeolian-deluvial and eluvial sediments of Buzkiy-Prychornomorskiy climatoliths. Alluvial sediments include yellow-grey, feldspar-quartz and quartz, diverse-grained, mainly fine- medium-grained, clayey, friable, in places ocherous sands. At the top the rocks in places contain interbeds (up to 1.0-1.2 m) of grey, brown-yellow sandy loams. Maximum thickness is 15.5 m (Sluch river nearby Glezne village). The rocks are not characterized by fauna and are defined by their hypsometric level, lithology and position in the column. After mineralogical analysis data, in some samples increased content of ilmenite, zircon, monazite and garnet is noted, as well as pyrope and chromospinelide signs. Kaydatskiy-Vytachivskiy climatoliths. Eluvial-deluvial sediments /edPII-IIIkd-vt/ in the geological map and cross-sections are shown as the single pedo-horizon because of quite limited development in the studied area of the cold phase sediments (Tyasminskiy and Udayskiy climatoliths) and their low thickness (less than 0.5 m). The total thickness is up to 0.6 m (Shybkiv village). Granulometric composition: less than 0.01 mm – 68.14%, 0.05-0.01 mm – 21.87%, 0.10-0.05 mm – 5.18%, 0.25-0.10 mm – 3.10%, 0.5-0.25 mm – 1.41%, 2.0-0.5 mm – 0.30%. Kaydatskiy-Prychornomorskiy climatoliths. Deluvial-aeolian and eluvial sediments /dv,ePII-IIIkd-pč/ are distinguished in the valley of South Boug river in the area of Goloskiv village and the sites Stavnytsya – Letychiv, Suslivtsi – Antonivka villages. The rocks overlie alluvial sediments or lie directly over eroded surfaces of the socle terraces. The footwall altitudes vary from +272.7 m (Verbka village) to +283.5 m (Stavnytsya village). The maximum thickness is noted in Stavnytsya village and comprises 4.2 m. The rocks include fine-micro-grained, brown and brown-yellow to light-grey sands, often with thin interbeds of brown-yellow, brown, yellow-grey sandy loam. Rarely grayish-yellow, grey, brown, friable, mainly non-carbonate sandy loams are observed. From the alluvial sediments they differ in fine sorting of clastic material and irregular coloring. Middle-upper branches undivided. Aeolian-deluvial and eluvial sediments /vd,ePII-III/. These rocks are distinguished in the eastern part of Litynskiy area where lie over Miocene sands and clays and over Pliocene red- brown clays. Thickness varies from 3.0 to 27.5 m. The rocks include yellow- and pale-grey, yellowish-brown, dark-brown, light and medium, in places sandy loams with interbeds of brown and dark-brown loams and sandy loams. The sediments are only shown in the lithological columns.

Upper branch

Of the all Pleistocene subdivisions, the rocks of Upper Neo-Pleistocene branch are most developed in the area. They are only absent in the river valleys and on the steep gully slopes. The rocks are intersected by a number of drill-holes and their surface exposures are noted in the most outcrops. In the sediments, sub-aerial facies predominate, including eluvial-deluvial soils of Prylutskiy, Vytachivskiy climatoliths, mapped within the complex of eluvial-deluvial sediments of Kaydatskiy-Vytachivskiy climatoliths, and aeolian-deluvial sediments of Buzkiy climatolith, mapped within the complex of aeolian- deluvial and eluvial sediments of Buzkiy-Prychornomorskiy climatoliths /vd,ePIIIbg-pč/. In Letychivska transitional valley and in Trebukhivskiy sub-area the deluvial-aeolian and eluvial undivided sediments of Buzkiy-Prychornomorskiy climatoliths are developed, and in 3-4th over-flood terrace – Vytachivskiy-Prychornomorskiy climatoliths. Sub-aqueous facies include only alluvial sediments of 1-2nd over-flood terrace of undivided Vilshanskiy-Desnyanskiy ledges. Prylutskiy climatolith. Eluvial-deluvial sediments /edPIIIpl/ are developed almost everywhere except most eroded sites in Letychivska transitional valley, Trebukhivskiy sub-area, and river valleys. They are mapped within the complex of eluvial-deluvial sediments of Kaydatskiy-Vytachivskiy climatoliths. The rocks lie over Kaydatski former soils and are overlain by Vytachivski soils, rarely – loams of Udayskiy climatolith. These are forest, meadow, meadow-forest, black-earth soils, dark-grey, brown-dark-grey, humused, medium-loamy, rarely heavy-loamy, dusty, in places with manganese spots and carbonate concretions at the bottom, 1.1-1.7 m thick in average. Udayskiy climatolith. Aeolian-deluvial sediments /vdPIIIud/ are locally developed in the interbeds 0.1- 0.3 m thick, rarely up to 0.5 m. They are mapped within the complex of eluvial-deluvial sediments of Kaydatskiy-Vytachivskiy climatoliths. The rocks everywhere lie over the soils of Prylutskiy climatolith. The footwall altitudes vary in the wide range from +273.9 (Chaplya village) to +345.7 m (Yaroslavka village). The rocks are mainly grayish-brown, brown-pale, light-brown loams, in some cases light-grey, medium, slightly dusty.

57 Vytachivskiy climatolith. Eluvial-deluvial sediments /edPIIIvt/ are developed almost over entire territory. They are mapped within the complex of eluvial-deluvial sediments of Kaydatskiy-Vytachivskiy climatoliths, and in the east of the area are defined as the separate straton. The rocks are absent at the elevated watershed parts of Trebukhivskiy (close to Lysogirka, Grushkivtsi villages) and Khmelnytskiy sub-areas. The rocks lie mainly over the soils of Prylutskiy climatolith from which they differ in specific weight and brown coloring; rarely they overlie aeolian-deluvial loams of Udayskiy climatolith. The footwall altitudes vary from +274.3 m (Chaplya village) to 354.2 m (Parkhomivtsi village). These are brown-earth, forest, medium- and heavy-loamy soils, often glued, dense, 0.8-1.4 m thick in average, rarely up to 3.4 m (Grechyntsi village). At the bottom somewhere carbonate concretions are noted. In Letychivska transitional valley (Dyakivtsi, Antonivka villages) Vytachivskiy climatolith consists of the meadow and meadow-swamp brown-grey and brown medium-heavy-loamy soils, dense, lumpy, in places ocherous and sandy. Quite often 2-3 horizons can be distinguished therein, which differ in coloring and structure. Buzkiy climatolith. Aeolian-deluvial sediments /vdPIIIbg/ do cover significant part of the territory with solid blanket, except the highest watershed sites and steep gully slopes in Litynskiy area and Trebukhivskiy sub- area. They are mapped within the single complex of aeolian-deluvial and eluvial sediments of Buzkiy- Prychornomorskiy climatoliths /vd,ePIIIbg-pč/ and in the east of map sheet area as the separate climato-straton. The rocks mainly lie over Vytachivski and Prylutski former soils, rarely over older rocks, and are overlain by the sediments of Dofinivskiy climatolith and the modern soils. The rocks are not characterized by fauna. The sediments include light, loess-like, yellow-pale, light-pale and brown-pale, dusty, somewhere sandy, in places with iron and manganese spots, calcareous loams with fine carbonate concretions. Thickness varies from 0.1 m (Yablunivka village) to 9.5 m (Yaroslavka village). The maximum thicknesses are noted at the watershed sites. By granulometric composition, the rocks include fractions: less than 0.01 mm – 59.18%, 0.05-0.01 mm – 35.27%, 0.10-0.05 mm – 4.38%, 0.25-0.10 mm – 0.94%, 0.5-0.25 mm – 0.16%, 2.0-0.5 mm – 0.07%. Dofinivskiy climatolith. Eluvial-deluvial sediments /edPIIIdf/ are mapped within the single complex of aeolian-deluvial and eluvial sediments of Buzkiy-Prychornomorskiy climatoliths /vd,ePIIIbg-pč/ and in the area between South Boug and Buzhok rivers and in the east of the map sheet it is distinguished as the separate straton. The rocks mainly lie over aeolian-deluvial sediments of Buzkiy climatolith, rarely over the soils of Kaydatskiy, Prylutskiy, Vytachivskiy climatoliths. These are mainly forest, brown, often glued, lumpy soils, dusty-medium-loamy, much rarely – light- and heavy-loamy, in the lower column part with the flint-carbonate concretions up to 1-3 cm in diameter. Their thickness is 1.4-2.2 m in average, maximum – up to 3.1 m (Chaplya village). The rocks are mainly distinguished by their position in the columns. Visually resemble Vytachivski soils. Prychornomorskiy climatolith. Aeolian-deluvial sediments /vdPIIIpč/ are mapped within the complex of aeolian-deluvial and eluvial sediments of Buzkiy-Prychornomorskiy climatoliths /vd,ePIIIbg-pč/. They lie over the soils of Dofinivskiy climatolith. The rocks are distinguished by their position in the columns, light mechanic composition and light coloring. These are light loams, grayish-pale to pale-grey, dusty, in places loess-like. In the transitional valleys and terraces they are sandy-dusty, often re-worked by the modern soil formation, very thin (0.2-0.3 m, in places up to 1 m). Vytachivskiy-Prychornomorskiy climatoliths. Deluvial-aeolian and eluvial sediments /dv,ePIIIvt-pč/ are developed in the 3-4th over-flood terraces of the South Boug and Buzhok rivers. They lie over alluvial sediments of Cherkaskiy-Trubizkiy ledges, and on lacking of the latter – over eroded surfaces of the socle terraces. The footwall altitudes vary from +271.7 to +273.2 m. These are mainly sands and sandy loams; yellow-grey and brown-grey, fine-micro-grained, quartz, in places with weakly visible banding, with sandy loam interbeds up to 10 cm thick. The total thickness is 1.3-2.1 m. From alluvial sediments differ in the fine sorting of clastic material and some irregularity in coloring. Buzkiy-Prychornomorskiy climatoliths. Deluvial-aeolian and eluvial sediments /dv,ePIIIbg-pč/ are developed in the southern part of the studied area. In Letychivska transitional valley they lie over alluvial and fluvio-glacial sediments of Dniprovskiy climatolith, rarely – over Vytachivski soils and eroded surface of Sarmatian clays, sands and limestones. In Trebukhivskiy sub-area they are mapped nearby Lysogirka village where lie over pre-Quaternary rocks. In Litynskiy area these rocks are only known in the south. The sediments are overlain by sand and sandy loam Holocene soils. The rocks are intersected by drill-holes and are observed in the outcrops. The footwall altitudes vary from +271.5 m (Verbka village) to 327.1 m (Lysogirka village). The rocks include light-grey and brown-yellow sands and sandy loams, rarely highly-sandy loams. The sands are quartz, fine-micro-grained, with minor clayey material and thin sandy loam interbeds (first centimeters). Sandy loams and loams are dusty, friable, non-carbonate. Thickness is 1.5-2.8 m, rarely up to 4.0 m (Verbka village).

58 Aeolian-deluvial and eluvial sediments /vd,ePIIIbg-pč/ are mapped as the single pedo-horizon because of wide distribution of aeolian-deluvial sediments of Buzkiy climatolith /vdPIIIbg/, low thickness of the sediments of Prychornomorskiy climatolith /vdPIIIpč/, and occurrence of eluvial-deluvial soil sediments of Dofinivskiy climatolith /edPIIIdf/ in the columns. Lithology and distribution are given in the description of mentioned climatoliths. The total thickness of the sediments is up to 12.3 m (Yaroslavka village). These sediments are accompanied by the deposits of construction materials (brick-tile raw materials) which are being mined for the local needs. nd Vilshanskiy-Desnyanskiy ledges undivided. Alluvial sediments of the 1-2 over-flood terrace /aPIIIvl-ds/ are locally developed and constitute Vilshanska-Desnyanska over-flood terrace of South Bough, Sluch rivers and their branches. The sediments mainly lie over the rocks of crystalline basement and their weathering crust, eroded surface of alluvial sediments of the 3-4th over-flood terrace, and over Sarmatian clays, sands and limestones, and in the area of Medzhybizh town, Stavnytsya, Goloskiv villages – over Paleogene sands and sandstones. The rocks include sands, from light-grey to brown, quartz and feldspar-quartz, diverse-grained, weakly- sorted, in places with oblique banding, at the top somewhere with brown-yellow, brown, grey sandy loam and loam interbeds. After mineralogical analysis results, in the area of Gorbasiv village increased content is noted for monazite – up to 5.08 kg/m3, ilmenite and leucoxene – up to 9.2 kg/m3, rutile and anatase – up to 0.11 kg/m3, as well as single grains of chromospinelides. Aeolian-deluvial and eluvial sediments /vd,ePIII/ are distinguished in the Northern peri-glacial sub- region where they constitute the slopes, watersheds and gullies. The sediments lie over the rocks of crystalline basement, and Neogene sands, clays and limestones. The rocks include loess-like, pale-yellow, yellow-grey, yellowish-brown, light and medium loams with sandy loam interbeds. Thickness varies from 3.0 to 26.0 m [12].

Pleistocene-Holocene divisions

Upper branch of Neo-Pleistocene section – Holocene division

Alluvial-deluvial sediments of gully bottom /adPIII-H/ are developed in the river flood-lands, gully and ravine bottoms. The rocks include brown-yellow and dark-grey to black loams, often with brown iron- enrichment spots, mainly thin-banded, sandy, dense, humused. In places they contain thin mud interbeds. Rarely diverse-colored sandy loams and sands are observed, spotty, often ocherous. Thickness is 1-2 m in average, rarely up to 5.8 m (Rossokhy village). Deluvial sediments /dPIII-H/ do cover the gully slopes with the solid blanket. They are exposed in the minor outcrops. The rocks include light and medium loams of variable coloring, spotty, friable, in places sandy, often with fine lumps of modern soil. Thickness normally does not exceed 1-1.5 m and is slightly increased at the slope foothills. In the scheme of Quaternary sediments and lithological columns the rocks are shown as the single undivided Upper Neo-Pleistocene – Holocene complex of deluvial sediments.

103Holocene division

Holocene sediments in the studied territory include diverse genetic types: eluvial, alluvial, lake-swamp, aeolian, technogenic, and biogenic. Eluvial sediments /eH/ include modern soils, which cover the older rocks with the solid blanket. Genetic type and lithology of soils depend on their position in the relief and composition of rocks involved in the soil formation. Most widespread are black-earths, meadow, sod-podzol forest, black-earth-meadow and swamp soils, Thickness of the modern soils varies from 0.1 to 3.0 m. Alluvial sediments /aH/ constitute the flood-land and course of rivers, gullies and ravines. They are developed in the valleys of South Boug, Buzhok, Ikva, Sluch, Derevychka, Khomora rivers. Thickness is not persistent and varies in the range from 0.8 to 14.0 m. The sediments of river-course and flood-land facies are distinguished. The river-course facies is developed along the major rivers and mainly consists of quartz and feldspar-quartz sands, diverse-grained, in places with pebble and gravel, weakly sorted, rounded in various extents, grey, light-grey, brown-yellow, often muddy. The flood-land facies sediments are variable in lithology – from sands to loams and mud-clay sediments. The dark-grey and brown, with ocherous spot, humused varieties predominate. Quite often thin- parallel banding is observed. Lake-swamp sediments /lbH/ are confined to the closed dimples, which are being periodically filled with the rain and melted waters. The rocks are developed in Lyubarskiy area and river terraces and transitional

59 valleys. The sediments are dark-brown, grey, dark-grey, with brown and ochreous spots, clayey, sandy-clayey and mud, up to 2 m thick. Aeolian sediments /vH/ are mapped at the surface of the South Boug terrace (Gorbasiv village). The sediments include light-grey, in places yellow-grey, fine-micro-grained, quartz sands, somewhere with minor clayey material. Thickness is up to 2.0 m. Technogenic sediments /tH/ are developed in the areas of inhabited localities, in places of mining works (dumps), construction of roads, dams, tailing ponds and irrigation units (channels, reservoirs). The quarries for construction materials are mainly located on the gully slopes, rarely on terraces or in the river flood-lands. Their dumps somewhere occupy considerable space. The sediments are sandy-clayey, gruss-sandy, or boulder heaps of artificial origin. Biogenic sediments /bH/ are developed in the river and their branches flood-lands. They include peat, peat-mud, mud-clayey, in places sandy, with swamp plant remnant sediments, brown, brown-grey, dark-grey, often iron-enriched, with brown spots. The maximum thickness is up to 5.0 m. The peat deposits are related to these sediments.

43. NON-STRATIFIED UNITS

Intrusive and ultra-metamorphic rocks were developing at the various stages of geological evolution. According to the valid Correlation chrono-stratigraphic scheme of Early Precambrian units in Ukrainian Shield, 2003, the following complexes are distinguished:

Proterozoic Eon Paleo-Proterozoic Era

Podilska LTZ Novograd-Volynska LTZ Dyke complex βPR1 - diabases νPR1 - gabbro-diabases Zhdanivska association of ultramafic rocks υσ, υPR1žd(?) - serpentinized peridotites, pyroxenites Proskurivskiy intrusive complex EξPR1pr - syenites, nepheline syenites EτPR pr - mafic phoidolites: melteigites, 1 jakupirangites, alkali pyroxenites υ,ν,ενPR pr - pyroxenites, gabbro, gabbro-norites, 1 sub-alkali gabbro, essexites Khmilnytskiy intrusive complex ap γ PR1hm - aplite-pegmatoid granites lγPR1hm - leucocratic granites Bukynskiy intrusive complex avPR1bu - amphibolized gabbro ενPR bu - gabbro-monzonites, gabbro- 1 norites, monzonites μδPR1bu - monzonites Zhytomyrskiy ultra-metamorphic complex γPR1zt - biotite and two-mica granites Berdychivskiy ultra-metamorphic complex ap γ PR1bd - aplite-pegmatoid granites lγPR1bd - leucocratic granites bt bt γ , γ mPR1bd - leucocratic granites γ, γmPR bd - garnet-biotite granites and 1 migmatites, often with cordierite pγ, pγmPR bd - garnet-biotite plagiogranites and 1 plagiomigmatites vnPR bd - garnet-biotite granites and migmatites 1 with hypersthene (vinnytsites) Sheremetivskiy ultra-metamorphic complex pγ, pγmPR šr - biotite plagiogranites and 1 plagiomigmatites γδPR1šr - amphibole-biotite plagio- migmatites of tonalite and granodiorite composition

Archean Eon Meso-Archean Era Litynskiy ultra-metamorphic complex

čAR2lt - charnockites enAR2lt - massive leucocratic enderbites

Paleo-Archean Era Gayvoronskiy ultra-metamorphic complex enAR1gv - banded gneiss-like enderbites, mainly of tonalite composition

Sabarivskiy intrusive complex

υAR1sb - amphibolized, serpentinized pyroxenites amvAR1sb - amphibolized gabbro, hornblendites

24Intrusive rocks

61Archean Eon

104Paleo-Archean Era

Podilska LTZ

Sabarivskiy complex (AR1sb)

Sabarivskiy intrusive complex includes minor bodies of metamorphosed mafic and ultramafic rocks intersected by drill-holes in the far south of the map sheet close to Gorbasiv, Pyrogivtsi villages [51]. These rocks are observed in association with Tyvrivska sequence meta-volcanics of Dnistersko-Buzka Series, being probably co-magmatic to the latter, and also in skialites within granitoids. The distinct feature of the rocks is essential secondary alteration of the rock-forming minerals: olivine and pyroxene replacement by amphibole, biotite, serpentine, talc, carbonates, and plagioclase – by scapolite. By composition the rocks include amphibolized gabbro and hornblendites (amvAR1sb), and amphibolized and serpentinized pyroxenites (υAR1sb), that is, these are mafic rocks of normal range. The similar rocks are described by P.F.Bratslavskiy [15] in the adjacent territory from the east in Ulanivska structure. In the drill-hole, located at the southern outskirt of Pyrogivtsi village [51], at the depth 71.0 m the greenish-black, medium-grained hornblendite is intersected consisting of amphibole and olivine relicts; the rock is probably developed after olivine pyroxenite. In minor amounts magnetite is observed. The processes of serpentinization, talcization and carbonatization of the rock-forming minerals are extensively developed. In the drill-hole in 1.5 km to the north-north-east from Gorbasiv village [51], at the depths 159.5-160.9 m and 176.1-176.8 m, the rock comprises grayish-dark-green, medium-grained, massive phlogopite-bearing pyroxenite, fine-grained and gneiss-like at the contacts. Under microscope the rock texture is lepido- nematoblastic, heteroblastic, poikiloblastic, gabbro-ophitic (in relicts). Mineral composition: pyroxene and plagioclase – by 30-85%, amphibole – 15-20%, mica – 5-10%; secondary minerals: talc, carbonate, scapolite, quartz, clay minerals; accessories: apatite, sphene; ore minerals: magnetite, ilmenite, sulphides (pyrite, pyrrhotite). Just the orthopyroxene (hypersthene?) is noted, quite irregularly distributed, with grain size 0.2-1.0 mm, and is normally replaced by green hornblende. In places the intergrowth textures of pyroxenes with amphiboles and talc (by fractures) are observed. The micas (phlogopite) are commonly orange-colored and developed after amphiboles, rarely – pyroxenes. Plagioclase (No. 45-52) of andesine composition is scapolitized. The micro-cracks between poly-synthetic twins are filled with clayey minerals and carbonates. The secondary processes had led to pyroxenite modification into the phlogopite-amphibole-pyroxene meta-mafic rock. In hornblendites, intersected by drill-hole nearby Pyrogivtsi village, the K2O content in ultramafic rocks, after silicate analysis, is 0.07%. Examination of the chemical composition allows the following conclusions: 1. High MgO content (21%) and considerable MgO excess over CaO (more than two times) suggest for significant depth of the given rocks formation (apparently, upper mantle origin). 2. Low K2O content and limited spatial development of Sabarivskiy complex rocks indicates that these rocks are only preserved at the sites with low granitization and least expressed metasomatism. By the content of micro-elements the ultramafic rocks of Sabarivskiy complex exhibit strong positive specialization for chromium and nickel.

62 By petrophysical parameters the hornblendites display slightly increased density (2.74 g/cm3) and high values of magnetic susceptibility (up to 4200×4π×10-6 CI units) and residual magnetization (2235×10-3 A/m). Pyroxenites, intersected by drill-hole nearby Gorbasiv village [51], are high-density (σ = 2.91 g/cm3) and increased magnetic susceptibility (209×4π×10-6 CI units). Even in cases of low thickness these rocks are expressed in positive magnetic and gravity anomalies.

62Proterozoic Eon

105Paleo-Proterozoic Era

Novograd-Volynska LTZ

Bukynskiy complex (PR1bu)

The rocks of Bukynskiy complex in the studied territory are intersected in the far north part, in the junction zone of Andrushivska and Teterivska zones of deep-seated faults. Intrusive rocks of the Complex include amphibolized gabbro, gabbro-monzonites and monzonites of Varvarivskiy massif and its apophyses and satellites in the area of Brazhyntsi, Vel. Derevychka, Kipchyntsi, Zhytyntsi villages, and also related dykes of gabbro-amphibolites. Varvarivskiy maric sub-alkaline massif is located at the border of two mega-blocks of Ukrainian Shield – Dnistersko-Buzkiy and Volynskiy. The massif shape is irregular, elongated in the sub-latitudinal direction. By drilling data [2], it is 9-9.5 km in size by the long axis and its maximum width is 2.7 km. In the southern envelope some satellite massifs of mafic rocks 2.5-3.0 km2 in size are encountered. The host rocks of Varvarivskiy massif include Paleo-Proterozoic Vasylivska Suite and ultra- metamorphic granitoids of both Sheremetivskiy and Berdychivskiy complexes. The rocks of Varvarivskiy massif are ascribed to Bukinskiy complex since they are quite similar to the latter rocks both in composition and age. Absolute age of Bukinski rocks [2] is 2000+30 Ma, and age of pyroxenites at Varvarivka village determined on zircons by U-Pb method – 1970-2010 Ma; absolute age of gabbro-monzonites in the given massif determined on biotite – 1950 Ma. The rock crystallization temperature calculated using biotite-orthopyroxene geo-thermometer of B.G.Yakovlev, is in the range 790-880oC, and oxygen activity is high – lgfO2 = 11.5-12.9 atm. Intrusive is layered in the hidden and visual modes, as it is evidenced by the numerous cumulate layers, which by mineral composition correspond to almost all rock varieties in the massif. Despite of high modal potassium feldspar content, just 10% of the rocks fall into the field of sub-alkaline rocks, which is caused by the high calcium content of plagioclases [20]. Two rock types can be distinguished: with iron number about 45% and MgO content 9-18%, and with iron number 60% and MgO content 4-8%. According to criteria of N.M.Chernyshov [8], Varvarivskiy massif is being treated as meso-abyssal, poly-phase, chamber-differentiated layered intrusion of high-magnesium magma. Just its upper part is intersected and there are all reasons to assume that at the depth it may have more magnesium composition, greater size and common with its satellites chamber. By the geophysical modeling results, the massif is 30 km long and 8.5 km wide in the western and 13.5 km – in the eastern parts. Varvarivskiy massif is analogue of Elan- Vyazivskiy pluton in Voronezkiy crystalline massif [20]. Below are given more details on the major rock varieties in Varvarivskiy massif. Gabbro-monzonites and gabbro-norite-monzonites (ενPR1bu) are mapped by drill-holes in the western and south-eastern parts of Varvarivskiy massif [20] and look like the endo-contact band 0.5-0.7 km wide. Further to the north-east (close to the northern map sheet border) these rocks are substituted by amphibolized gabbro (aνPR1bu). Macroscopically gabbro-monzonites and gabbro-norite-monzonites are grey or greenish-grey medium- grained rocks. Under microscope: texture is hypidiomorphic with elements of monzonitic. Mineral composition: plagioclase (No. 50) – 35-60%, potassium feldspar – 5-25%, orthopyroxene – 5- 30%, clinopyroxene – 3-10%, hornblende – 1-10%, biotite – 3-5%. Amphibolized gabbro differs in melanocratic appearance, lack of potassium feldspar and content of hornblende, replacing pyroxenes, up to 20%. Plagioclase (andesine-labrador) is observed in idiomorphic-tabular grains 1.5-2.0 mm in size, with curvilinear-jagged contours, highly saturated with numerous antiperthite intergrowths with thin poly-synthetic twins under albite rule.

63 Potassium feldspar – micro-perthite is observed in strongly xenomorphic grains in between plagioclase crystals and somewhere contains ingrowths of the latter. Pyroxenes (mainly hypersthene) are uniformly distributed in almost isometric grains 0.15-1.5 mm in size, slightly fractured. Pyroxene is often rimmed by xenomorphic grains of deep-colored hornblende. Biotite is brown, dark-brown, observed in irregular broad laths surrounded by scarce grains of ore mineral. In the rock the short-prismatic and isometric grains of apatite up to 0.1 mm in size are permanently observed located in around of pyroxene grains. Fine xenomorphic grains of quartz are also noted in amount up to 2-3%. The petrochemical parameters of the rocks are given in Table 3.1.

Table 3.1. Petrochemical parameters of the rocks of Bukynskiy complex

Granitized gabbro (νPR bu) Gabbro-monzonite (νξPR bu) Oxides, ratios 1 1 X, % Min Max X, % Min Max SiO2 56.94 54.92 58.96 56.75 53.70 59.45 TiO2 0.94 0.87 1.01 0.74 0.60 0.92 Al2O3 15.90 15.83 15.96 14.99 13.78 15.75 Fe2O3 1.29 1.00 1.57 1.50 0.76 2.18 FeO 6.11 5.23 6.98 6.08 4.78 6.91 MnO 0.05 0.01 0.10 0.13 0.12 0.14 MgO 3.68 3.36 4.00 6.70 3.49 10.75 CaO 6.31 5.49 7.13 5.16 4.37 6.06 Na2O 3.55 3.36 3.74 3.14 2.73 3.34 K2O 2.10 1.00 3.20 2.56 1.30 3.62 - H2O 0.18 0.10 0.25 0.06 - 0.20 P2O5 1.40 0.46 2.33 0.43 0.30 0.72 SO3 0.35 0.31 0.39 0.09 0.05 0.22 Sum 99.55 99.53 99.56 99.57 99.52 99.70 f 1.10 1.10 1.10 0.62 0.39 1.09 Is 47.00 40.00 54.00 52.00 41.50 61.00 Na+K/Al 0.51 0.46 0.56 0.53 0.45 0.59 Oxides, ratios Monzonites (ξPR1bu) Gabbro (vPR1bu) SiO2 X, % Min Max X, % Min Max TiO2 60.04 55.77 64.31 52.16 52.04 52.27 Al2O3 1.17 1.03 1.30 0.32 0.31 0.32 Fe2O3 15.49 15.38 15.60 11.46 11.06 11.85 FeO 2.69 2.65 2.72 1.33 0.97 1.69 MnO 4.57 2.73 6.40 7.36 7.29 7.43 MgO 0.09 0.05 0.14 0.15 0.15 0.15 CaO 2.48 1.49 3.46 13.51 13.39 13.63 Na2O 4.97 3.71 6.23 9.50 9.44 9.55 K2O 3.94 3.86 4.01 1.64 1.60 1.67 - H2O 2.41 2.19 2.62 0.48 0.47 0.49 P2O5 0.14 0.02 0.25 0.16 0.12 0.20 SO3 0.53 0.39 0.68 0.02 0.02 0.02 Sum 0.14 0.06 0.21 0.20 0.19 0.21 f 99.72 99.54 99.89 99.44 99.40 99.47 Is 1.58 1.42 1.95 0.36 0.34 0.37 Na+K/Al 56.00 51.00 62.60 18.20 18.10 18.30 0.59 0.58 0.60 0.28 0.27 0.29

Note: X – mean oxide content in % in range of values – minimum (Min) and maximum (Max). 2  )OKONa(100  KNa Fe*100 - iron number in %; Is  2 2 - salic index; - agpaite coefficient. f  2  MgFe 2  2OKONaCaO Al

64 In the gravity field the gabbro-monzonites of Varvarivskiy massif are expressed in the positive ring anomaly 0.5-1.0 mGal in amplitude 4×2 km in size; in the eastern part the ring anomaly is 2.5×1.6 km in size and 0.4-1.3 mGal in amplitude.

By the patterns of magnetic field and Ta anomaly intensity the massif is also divided in two parts – the western and eastern ones – by line of Brazhyntsi – Duboviy Gay villages. The western part contains linear and elliptic positive magnetic anomalies 0.5-2 km in size arranged in the semi-ring structure. The anomaly amplitude varies in the range 500-900 nTl. Magnetic anomalies in the eastern part are mainly intricate or elliptic and are observed along the endo-exo-contact of the massif’s rocks. Amplitude of magnetic anomalies is 50-300 nTl. 3 Petrophysical parameters: gabbro-monzonites display increased density σavg. = 2.90 g/cm , magnetic -6 -3 susceptibility – æavg. = 307×4π×10 CI units, residual magnetization – Ir = 400×10 A/m, which are slightly higher than those parameters of Bukynskiy massif. Monzonites (μδPR1bu) comprise the most widespread rocks in Varvarivskiy massif and constitute more than 80% of its square. Macroscopically these are grey, dark-grey with slight greenish shade, fine-medium-grained, massive rocks. The composition and structure-texture features allow classifying these rocks as mangerites [20] and in this respect they differ from the similar rocks of Bukynskiy massif. The typical monzonites of Bukynskiy massif do have monzonitic and poikilitic texture and are composed of andesine – 40-60%, potassium feldspar – 25-40%, quartz – 3-10%, clinopyroxene – 0-10%, orthopyroxene – 5-15%, biotite – 3-10%, and hornblende – 1-15%. In Varvarivskiy massif these rocks exhibit hypidiomorphic with elements of ophitic, in places monzonitic, micro-texture. Structure is massive. Mineral composition: plagioclase (andesine) – 35-70%, orhtopyroxene – 15-40%, clinopyroxene – 5-15%, potassium feldspar – perthite – 5-15%, quartz – 0-5%, biotite – 0-5%, apatite, ore minerals. The rocks are composed of idiomorphic-tabular grains of intermediate plagioclase, uniformly distributed opaque minerals and minor amount of potassium feldspar – perthite and quartz. The crystal size is normally 1-1.5 mm, some plagioclase grains attain 2.5 mm by long axis. Plagioclase edges are curvilinear-jagged, it contains fine antiperthite ingrowths, in places with unclear zonation. Orthopyroxene (hypersthene) is observed in short-prismatic and isometric grains, both individual and in the intergrowths with clinopyroxene and hornblende. Clinopyroxene is developed in the isometric grains with curvilinear edges. Hornblende is brown-green, observed in irregular grains along the pyroxene margins. Potassium feldspar – perthite is developed in strongly xenomorphic grains. Quartz is rarely noted than potassium feldspar in xenomorphic grains. Ore minerals include irregular grains and are associated with opaque minerals; often they are overgrown by biotite. Petrophysical properties of these rocks, according to previous authors, almost do not differ from those 3 -6 -3 of gabbro-monzonites: σavg. = 2.85 g/cm , æavg. = 372×4π×10 CI units, Ir = 523×10 A/m [94]. In the gravity field, on the background of gabbro-monzonites, the monzonites are expressed in the low- amplitude negative anomalies δga. In the western part of Varvarivskiy massif the monzonites display linear high-gradient magnetic field reflecting the deep structure of intrusion. In the eastern part of massif the field Ta is differentiated, with numerous alternating anomalies from first tens to 200-400 nTl in amplitude. The petrochemical parameters of the rocks are given in Table 3.1. The minor satellites of Varvarivskiy massif are also composed of gabbro-monzonite rocks. The dykes, apparently, have been formed coevally with these rocks and probably comprise the final phase of specific stage in the intrusive activity. The dykes are composed of gabbro-diabases. It is interesting that above gabbro-monzonite massifs the vermiculite weathering crust is developed: in drill-hole nearby Brazhyntsi village hydromica content is 85% and vermiculite – 17.69%. By the geochemical specialization the mafic dykes, distinguished by P.F.Bratslavskiy in Malobratalivska site, A.S.Voynovskiy [18] has suggested to ascribe to Bukynskiy complex. Visually the mafic rocks are dark-grey with greenish shade, uniformly micro-fine-grained, massive, in places unclear-banded. The contacts with host rocks (charnockitoids of granodiorite composition) in places are sharp and somewhere – gradual. Texture is granoblastic, hetero-lepido-granoblastic, nemato-granoblastic. Structure is parallel, in places layered. Mineral composition (%): plagioclase (No. 30-47) – 60, amphibole – 16-37, biotite – 8-20, microcline – up to 5, quartz – up to 2, pyroxene – single grains. These rocks are extensively re-crystallized and this is expressed in almost complete replacement of pyroxenes by amphiboles and K-feldsparization.

65 P.F.Bratslavskiy considers these rocks the dyke ones, from the one hand, and does not exclude, from another hand, that they comprise the final products of enderbite de-basification. At the same time, texture-structure features of these rocks are not characteristic for intrusive rocks; in addition, by chemical composition they differ from the typical rocks of Bukynskiy complex. These reasons, coupled with their setting within charnockites of Litynskiy complex, allow assumption that these rocks comprise metasomatically altered meta-volcanics of Dnistersko-Buzka Series.

Podilska LTZ

Khmilnytskiy complex (PR1hm)

The studies of the rocks, which under the modern chrono-stratigraphic scheme belong to Khmilnytskiy complex, have been conducted by V.I.Luchitskiy, L.G.Tkachuk, Yu.I.Polovynkina, M.P.Shcherbak. M.P.Shcherbak [11], based on analysis of large amount of collected information on Khmilnytski granitoids, has given an idea (the present authors also support which) that these rocks belong to the separate complex of allochthonous granites, developed in the conformable and cutting bodies and minor massifs within the rocks of gneiss sequence and Berdychivski granitoids; they have distinct composition and are somewhat younger than Berdychivski rocks. ap Khmilnytskiy complex includes leucocratic (lγPR1hm), pegmatoid and aplite-pegmatoid (γ PR1hm) granites developed in Khmilnytskiy massif and its satellites. The massif is located in the cross-junction of Khmilnytska and Yablunivsko-Bilokorovytska deep-seated fault zones. The massif size is 10×14 km (by geophysical data). Khmiltynski granitoids are studied in the outcrops [51, 54] and in drill-holes [47, 51] in the area of Khmilnyk town and its outskirts. In the map of crystalline basement generalized, with regard to the map scale, area of the Complex rocks distribution where the oldest rocks (mainly Berdychivski granitoids) are preserved in the minor remnants and xenoliths. Leucocratic granites strongly predominate in the massif. They are tightly associated with Berdychivski granites and migmatites, normally having gradual transitions to the latter, and rarely the cutting contacts are noted. In Krutnivskiy quarry, where this granite petrotype is exposed, the gradual transitions are observed from Berdychivski garnet-biotite granites to leucocratic Khmilnytski granites. This transition is accompanied by the gradual lightening of Berdychivski granites, decreasing in biotite amount, microcline appearing, and garnet amount and grain size decreasing. Macroscopically leucocratic granites are pink, pink-grey and light-grey, diverse-grained, mainly medium-grained, massive or slightly-banded. Under microscope rock structure is granitic, pegmatoid or cataclastic. Mineral composition (%): quartz – up to 40, microcline 0 micro-perthite – 45, plagioclase (albite- oligoclase) – 15, biotite – single grains, garnet – single grains; accessories: apatite, monazite, zircon, sillimanite. Quartz is the major rock-forming mineral occurring in xenomorphic grains with abrupt wavy or mosaic extinction. Feldspars include micro-perthite and sodium plagioclase. Micro-perthite is almost always non-lattice and developed in grains 2-5 mm in size. Rarely microcline- perthite is noted. Micro-perthite grain contours are curvilinear, often albitized. Plagioclase – albite-oligoclase is irregularly distributed and shaped, often with quartz myrmekites, and also as relicts in myrmekite. Biotite is dark-brown, arranged in the flake streams. Increased, in comparison to biotite from Chudnovo-Berdychivski granites, fluorine content indicates high temperature (about 700oC) [10] of this biotite formation. Garnet is permanently observed in the rounded grains from 0.1 to 2 mm in size, rarely up to 1.5 cm. Color is pale-pink. Refraction parameter is 1.773-1.795. Average garnet composition from leucocratic granites of the Complex [2] (%): almandine – 69.16, spessartite – 11.11, pyrope – 26.22, andradite – 2.81. In comparison to the garnet from Chudnovo-Berdychivski granites or garnet from the rocks of Khmilnytskiy complex, the given garnet contains more pyrope indicating higher temperature of its formation. Apatite is observed in the grains 0.05-0.1 mm in size, color-less, or greenish-bluish. Monazite and zircon are permanently observed in grains 0.05-0.7 mm in size. Color is yellowish-brown. Monazite content in Khmilnytski leucocratic granites is higher in comparison with other granites in the territory. Sillimanite is developed in the needled grains in the gneissose varieties of granites. Secondary minerals were developing under low-temperature processes in granites resulted in formation of chlorite and rutile at the expense of biotite, and sericite and kaoline after feldspars. Chemical composition of leucocratic granites is given in Table 3.2.

Table 3.2. Average chemical composition of leucocratic granites of Khmilnytskiy complex

Leucocratic granites (lγPR hm) Oxides, ratios 1 X, % Min Max SiO2 71.96 69.00 74.64 TiO2 0.35 0.05 0.72 Al2O3 13.95 12.60 14.98 Fe2O3 0.91 0.12 1.61 FeO 2.35 0.43 4.20 MnO 0.06 0.01 0.07 MgO 1.74 0.45 2.88 CaO 1.61 0.39 2.39 Na2O 3.10 2.02 3.52 K2O 3.21 0.86 6.48 + H2O 0.14 0.03 0.39 P2O5 0.18 0.06 0.41 SO3 0.15 0.02 0.24 Ssulf. 0.02 - 0.06 CO2 0.01 - 0.07 Sum 100.43 99.40 102.43 4 6 V3 2.3×10 348 14×10 V4 3.51 0.03 1310 Na2O+K2O 6.31 4.33 9.47

2 2 2  2 )O(K)SiO( V3  - geochemical coefficient of granitization degree;  TiOCaOMgOFeO 2 )O(K 2 V  2 - geochemical coefficient of granitoids. 4  CaOMgOFeO See Table 3.1 for other legend symbols.

Absolute age determination data for Khmilnytski granites are in the range 2100-1900 Ma, that is, they are younger than Chudnovo-Berdychivski granites. Aplite-pegmatoid granites and pegmatites are commonly observed in the fields of leucocratic granites of the same complex, being arranged in the thin branched veins and veinlets, both conformable to the general host rock strike (to the south from Verbivka, Zhdanivka villages) and cutting ones (Krupyn, Kumanivtsi villages). Within Chudnovo-Berdychivski granites aplite-pegmatoid granites and pegmatites are scarcely observed (to the west from Dumenky, N.Synyavka, Tessy, Kozhukhiv villages). Normally these granites are confined to the zones of tectonic breaks, along which they have been emplaced and where then they underwent cataclasm and milonitization, or to the weakened zones along the host rock bedding. The body shape of aplite-pegmatoid granites and pegmatites is variable: large sub-conformable bodies, cutting and conformable veins, network of branched veinlets, injections by bedding. Thickness varies from the hair veinlets and veins 10-30 cm thick to the winding bodies up to 300 m thick and 1-3 km long (Kumanivtsi, Krupyn villages). At the boundary with granites under consideration, all crystalline rocks become enriched in potassium feldspar and pink coloring. Aplite-pegmatoid granites and pegmatites are the lightest rocks of Khmilnytskiy complex: density is 2.63 g/cm3; magnetic susceptibility – 99×4π×10-6 CI units; residual magnetization – 287×10-3 A/m. The gravity and magnetic fields caused by these rocks, in general do not differ from the field provided by the leucocratic granites. In the zones of tectonic breaks in some cases aplite-pegmatoid granites can be identified (because of low rock density) after the linear negative gravity anomalies δga, coinciding with negative magnetic field. Mineral composition of aplite-pegmatoid granites and pegmatites is uniform enough and inconsistent in term of the rock-forming mineral ratios. The rocks are composed of potassium feldspar, oligoclase, quartz, biotite, garnet, and accessories – monazite and zircon.

67 Characteristic rock structures are pegmatoid, cataclastic and blasto-milonitic. The graphic texture is rare. The rocks with pegmatite texture are irregularly-grained, with coarse potassium feldspar grains. Quartz is xenomorphic and fills up the inter-granular space. Garnet is observed in isometric grains 0.5-3 mm in size and in places coarse grains up to 1 cm in size are noted. The widespread tectonic processes had caused almost permanent development of cataclastic textures. Normally aplite-pegmatoid granites with these textures are thin – from 0.2 to 2 m, rarely 10 m, and exhibit augen structure. The bodies 20-100 m thick are known composed of pink coarse-grained “augen” aplite-pegmatoid granites and confined to the zones of tectonic breaks. The “augens” contain potassium feldspar grains and the inter-granular space is filled with crushed re- crystallized mass consisting of potassium feldspar and quartz. Biotite commonly surrounds the feldspar “augens” and in contained in the groundmass in the folded flakes. Accessory monazite is confined to the sites of fine-aggregate feldspar, quartz and biotite accumulations and is observed in the isometric grains 0.05-0.7 mm in size. Monazite formation is related [11] to metasomatic reworking of aplite-pegmatoid granites in the zones of tectonic breaks. In the cataclastic augen varieties of aplite-pegmatoid granites the apatite is developed in grains and irregularly-shaped bunch-like accumulations up to 0.5-1 cm in size. Apatite grains are bluish-greenish or greenish-yellowish. Refraction parameters are as follows: Np1 – 1.634, Ng1 – 1.637. Increased content of cerium-group rare-earths is characteristic for apatite. Apatite formation, like monazite one, is apparently related to the late metasomatic processes which have been extensively developed in the tectonic zones.

Proskurivskiy complex (PR1pr)

Proskurivskiy complex includes diverse in composition and chemistry intrusive rocks displaying evidences for the alkali-gabbroid formation affinity. The time of their formation, geodynamic conditions, structure-tectonic control are common. The rocks are developed in Khmelnytska tectonic zone, in the sub- latitudinal band more than 40 km long and about 15 km wide. Individual massifs and their groups in the central part of this band are confined to the cross-junctions of Khmelnytska zone with the north-west-trending faults: Romanivskiy, Letychivskiy and Rudnyanskiy, constituting three separate fields (from the east to west): Antonivske, Rudnyanske and Goloskivske. Mainly based on results of DGM-50 [51] by geophysical data some tens of minor bodies and massifs (up to 5-6 km2) are distinguished and partially proven by drilling. Most studied, also by structure-prospecting drill-holes, are Antonivskiy and Goloskivskiy massifs.

Antonivskiy massif

The massif is encountered in the course of DGM-200 [159] and then studied during prospecting works for apatite [58]. The massif is located to the south-west from the same-named village. It is elliptic in shape and extended in the north-western direction by 4 km being 1.5 km wide. The massif is confined to the cross-junction of the sub-latitudinal and north-western (Romanivskiy) tectonic breaks. The massif is composed of the rocks of alkaline-ultramafic range: essexites, alkaline pyroxenites and jakupirangites, ijolite-melteigites, and nepheline syenites. Below generalized columns are given by the structure-prospecting drill-holes drilled in Antonivskiy massif [58]. The data processing is performed under participation of S.G.Kryvdyk. Drill-holes intersected the central and contact parts of the massif and the north-eastern contact with granites of Berdychivskiy complex.

DH 189 Depth, m 1. Feldspar-pyroxene rocks like thwaitosite and non-nepheline essexites 38.3-59.7 Nepheline syenites and juvites with melanocratic rock enclaves (up to 10 m), ijolite- 2. melteigite rocks at the depths: 63.2-65.4; 66.0-71.3; 75.3-76.1; 79.0-81.2; 85.9-88.1; 59.7-197.2 89.3-92.1; 102.1-105.1; 110.0-112.8; 113.0-114.1; 114.8-119.0; 119.4-120.1 m 3. Apo-granite phenites pf syenite composition with single veins of nepheline syenites 197.2-303.0 DH 190 1. Ijolites, juvites with nepheline syenite veins 44.0-119.9 2. Nepheline syenite 119.9-158.0 3. Phenites with essexite intervals (159.9-160.0; 205.5-205.9; 207.3-207.6 m) 158.0-213.6 4. Jakupirangites with essexite enclaves and ijolite veins 213.6-264.0 5. Nepheline syenite 264.0-267.0

68 DH 191 Depth, m 1. Apo-granite phenites 45.2-67.4 2. Non-nepheline essexite with pyroxenite and phenite enclaves 67.4-143.0 3. Phenites 143.0-202.3 4. Cataclased, altered essexite 202.3-228.0 5. Alternating nepheline essexites and nepheline syenites 228.0-254.0 6. Phenites with essexite and nepheline syenite veins 254.0-322.1 7. Non-nepheline essexites 322.1-346.0 8. Ijolite-melteigites 346.0-350.0 9. Nepheline syenites 350.0-359.8 10. Pyroxenites, jakupirangites with nepheline syenite veins 359.8-366.5 11. Nepheline syenites 366.5-380.0 12. Phenites 380.0-402.5 13. Intercalation of pyroxenites, jakupirangites with nepheline syenites 402.5-440.0 14. Alkaline pyroxenites, jakupirangites 440.0-496.6 15. Nepheline syenites 496.6-519.5 DH 196 1. Alkaline pyroxenites and jakupirangites with ijolite and melteigite veins 30.0-90.0 2. Pegmatoid alkaline syenites 90.0-107.3 3. Juvites, ijolite-melteigites 107.3-118.9 4. Pegmatoid alkaline syenites 118.9-126.4 5. Non-nepheline essexites 126.4-140.5 6. Pegmatoid alkaline syenites 140.5-155.5 Non-nepheline essexites with pegmatoid syenite veins; at the depths 155.1-157.0 m 7. 155.5-204.5 and 200.5-203.5 m – ijolite-melteigites 8. Jakupirangites, pyroxenites with non-nepheline essexite and phenite enclaves 204.5-310.0 DH 197 1. Non-nepheline essexites with phenite enclaves 28.5-66.9 Phenites and phenitized granites with thin intervals of non-nepheline essexites; at the 2. 66.9-130.0 depth 166.9-122.0 m – zone of cataclasm 3. Phenitized granite with scarce garnet and biotite grains 130.0-165.0 Leucocratic biotite-garnet-bearing granite with xenoliths of garnet-biotite mafic 4. 165.0-252.0 gneisses

Besides structure drill-holes, the massif rocks are also studied in the deep geochemistry drill-holes [23, 51]. Based on results of these studies, some regularities in the massif structure should be noted. In the endo- contact portion the essexites (mainly non-nepheline varieties) are commonly developed. In the central part the alkaline pyroxenite-jakupirangites, ijolite-malteigites and nepheline syenites predominate which constitute the thickest bodies in the massif core. All mentioned types of alkaline rocks often alternate with phenites. Chemical composition of major massif rock varieties is given in Table 3.3. In the massif exo-contacts phenite aureole is clearly expressed in the hosting granitoids. The minor massifs and bodies in Antonivske and Rudnyanske fields are less complicated in structure. They are mainly composed of syenites and quartz syenites, and around the biggest ones phenitization aureoles are also distinguished. Sub-alkaline and alkaline mafic rocks are much rarely developed. They are studied in Rudnyanska, Verbkivska and Antonivska sites.

Table 3.3. Average chemical composition (%) and petrochemical parameters of major rock varieties of Antonivskiy massif

Alkaline Nepheline pyroxenites Ijolite- Oxides, ratios Essexites syenites and Syenite Phenite and melteigites juvites jakupirangites SiO2 47.73 45.81 44.44 47.88 62.48 63.26 TiO2 1.94 1.83 1.24 0.63 0.22 0.54 Al2O3 13.26 7.45 19.04 21.17 17.98 14.08 Fe2O3 2.74 4.24 3.46 3.24 0.90 0.36 FeO 8.18 9.34 5.74 4.23 1.50 6.10 MnO 0.19 0.25 0.17 0.12 0.03 0.10 MgO 6.45 8.87 4.03 1.96 0.30 3.78 CaO 10.24 15.34 8.38 4.85 2.91 2.24 Na2O 3.82 2.73 7.12 8.55 5.88 5.46 K2O 2.05 0.97 2.68 3.96 5.96 2.66 P2O5 0.52 0.59 0.89 0.65 0.86 0.16 SO3 0.32 0.26 0.12 0.04 - 0.14 CO2 0.98 0.99 0.92 1.32 0.28 0.67 F - 0.23 0.19 - - - H2O 0.22 0.13 0.27 0.09 0.12 0.04 LOI 0.92 1.04 1.10 0.72 0.18 0.38 Sum 99.56 100.07 99.79 99.41 99.63 99.97  MnFe 0.476 0.45 0.556 0.675 0.517 0.489  MgMnFe  KNa 0.64 0.75 0.77 0.87 0.80 0.84 Al Na2O+K2O 5.87 3.70 9.80 12.51 11.84 8.12 ONa 2 1.86 2.81 2.66 2.16 0.986 2.05 2OK Number of 10 16 5 5 1 1 analyses

The apatite-bearing rocks intersected by DH 1585 [51] in Verbkivska site are of particular interest (from top to bottom):

Depth, m Pyroxene-biotite syenite, light-grey with greenish shade, coarse-grained, irregularly- 1. grained, contains little xenoliths (up to 10 cm thick) of biotite, exstensively K- 17.5-22.7 feldspatized gneiss Grey shonkinite (orthoclase gabbro), medium-grained, with fine apatite dissemination, at the end of run apatite content attains 2-4%. Composition: K- 2. 22.7-25.7 feldspar (orthoclase) – 40%, clinopyroxene (diopside-salite) – 30-35%, biotite – 15- 20% 3. Pyroxene-biotite, pink-light-grey, coarse-grained syenite 25.7-31.0 Orthoclase, light-green, fine-grained to medium-grained, apatite-bearing pyroxenite. 4. Composition: diopsidic clinopyroxene with admixture of biotite (5%), orthoclase 31.0-34.0 (5%) and apatite (2-3%), in places amphibole Greenish-grey, from fine- to medium-coarse-grained, massive, spotty shonkinite. Xenoliths of extensively granitized gneisses are noted. The rock is cataclazed. 5. Contains fine apatite dissemination. In composition is identical to the sample in run 34.0-55.5 22.7-25.7 m; in places brown-green amphibole appears, contains 1-2% of sulphides (pyrite, pyrrhotite)

In the deep-geochemistry drill-hole [51] at the depth 21.0-24.5 the weathering crust of mafic composition is intersected, and at the depth 24.5-29.5 m – greenish-grey, medium-coarse-grained spinel clinopyroxenite composed of diopsidic (colorless in thin sections) pyroxene (about 90%) and montmorillonite pseudo-morphs, apparently after olivine. Pyroxene contains fine (up to 0.3 mm) sub-idiomorphic inclusions of transparent green spinel (not more than 1% in total), and fine clayey mineral inclusions. Ilmenite is noted. Essexites (ενPR1pr) comprise gabbroids of oligoclase-barkevikite-salite composition with minor biotite, apatite and calcite. The rocks include massive and trachytoid medium-, rarely coarse-grained varieties. Plagioclase content varies from 10 to 40%, pyroxene – 30-60%, amphibole – 5-30%, biotite – 5-15%. Minor and accessory minerals: calcite (0.5-5%), apatite (0.5-1.5%), ilmenite, sulphides. In the internal parts of massif the nepheline (up to 20%) varieties of gabbroids appear, but in general non-nepheline varieties strongly predominate. Pyroxene, by chemical analyses [51], is comprised of aegirine-bearing salite or salite. In the nepheline varieties of essexites the greenish-brown pyroxene (titanium augite) is observed. Barkevikite is brownish. In the essexites from the outer zone of Antonivskiy massif the amphibole consists of high-alkali titanium hastignsite. Biotite exhibits extensive brownish pleochroism and comprises titanium variety. Plagioclase (oligoclase or albite No. 9-10) is often more xenomorphic than clinopyroxene but more idiomorphic than amphibole. Alkaline pyroxenites and jakupirangites (EτPR1pr) comprise medium-, rarely fine-grained dark-colored rocks of massive and directive structure. They are composed of pyroxene by 70-90%, which is somewhere replaced by barkevikite, titanium hastingsite and biotite, as well as minor plagioclase, nepheline and calcite. Characteristic accessory minerals include ilmenite and apatite. Both in alkaline pyroxenites and jakupirangites clinopyroxene is comprised of aegirine-bearing salite. Alkaline pyroxenites and jakupirangites apparently are one of the earliest rocks in the massifs of Proskurivskiy complex but their relationships with essexites described above are not clearly defined yet. Ijolite-melteigites (EτPR1pr) are encountered in the thin veins in essexites, alkaline pyroxenites and remnants within nepheline syenites. Mesocratic varieties (with approximately equal amounts of nepheline and pyroxene) predominate – ijolites and feldspar ijolites. Of the ijolite-melteigites the medium-grained varieties predominate with well enough expressed trachytoid patterns. Pyroxene is aegirine-salite. Feldspars include oligoclase-albite or micro- or meso-perthite feldspar like anorthoclase. Minor minerals: amphibole, biotite, apatite, calcite. In melanocratic varieties ilmenite is noted. Nepheline syenites (EξPR1pr) are noted frequently enough in the thin veins and veinlets within all rocks of the complex. Somewhere their bodies are thick enough (25-50 m). Macroscopically the medium-fine-grained gneiss-like and massive, as well as coarse-grained to pegmatoid varieties of nepheline syenites are distinguished. Their texture is regularly-grained or porphyry-like. Opaque minerals include aegirine-salite, green and brown- green hastingsite and biotite. Alkaline feldspar in nepheline syenites includes micro- and meso-perthite varieties where albite phase (anorthoclase) predominate. By the ratio of nepheline to feldspar juvite (nepheline predominate), foyaite and pulaskite (few nepheline) varieties are distinguished. In general, foyaites predominate. Juvites are probably related to the feldspar ijolites. Pyroxene syenites ands nepheline syenites of Antonivskiy massif are less dense (2.69-2.72 g/cm3) than sub-alkaline mafic rocks, similar high magnetic susceptibility in samples taken in the south-western part, and probably lesser one in the north-eastern part. After the density modeling results [58], the depth of Antonivska structure is 0.78-1.0 km. Phenites, alkaline syenites, syenites and quartz syenites (EξPR1pr). These rocks are grouped together because of gradual transitions between them although they differ in structure-texture features and modes of origin. The alkaline syenites are locally developed. These include coarse-grained to pegmatoid pyroxene syenites, most developed in the central part of Antonivskiy massif. In syenites the alkaline feldspar is orthoclase- perthite. Most of leucocratic and in lesser extent mesocratic rocks of syenite composition are thought to be apo- granitic phenites. These phenites are developed in the contact, rarely in the central parts of Antonivskiy massif and separate the alkaline and sub-alkaline mafic rocks described above from the host granitoids, and also constitute the minor bodies and massifs. Syenites (phenites), quartz syenites, alkaline syenites are the rocks with least density and almost non- magnetic. Average density value is 2.63 g/cm3, the range (for 80% of samples) is from 2.55 to 2.67 g/cm3. -6 Magnetic susceptibility in 90% of samples does not exceed 70×4π×10 CI units, the modal value æavg. = 11×4π×10-6 CI units. Histogram of residual magnetization is bimodal and two groups can be distinguished: 60% -3 -3 of samples exhibit low residual magnetization (modal value Ir = 0.5×10 A/m), and in 35% Ir = 10×10 A/m.

71 In the gravity field the rocks are expressed in the local small-size (0.5-1.0×0.7-2.0 km) minimums, oval, isometric or extended along the fault lineaments, 0.25-0.75 mGal in amplitude. These minimums are mainly defined by the results of the mapping in the scale 1:10 000. 3 Alkaline gabbroids (ενPR1pr), intersected in Verbkivska site, exhibit high density (σavg. = 2.94 g/cm ) -6 and low magnetic susceptibility (æavg. = 53×4π×10 CI units). However, looking at the magnetic field, these rocks are high-magnetic. By the results of detailed gravity-magnetic surveys in the scale 1:10 000 they are expressed in the positive magnetic anomaly up to 1500 nTl in amplitude, which coincides with the local gravity anomaly 0.25 mGal and higher in amplitude. Sub-alkaline mafic rocks of Antonivskiy massif display high values of density (from 2.90 to 3.19 g/cm3, 2.96 g.cm3 in average) and magnetic susceptibility (from 2 to 8 thousand ×4π×10-6 CI units) [58]. In the gravity field they are expressed in elliptic high-intensity δga maximum (more than 2.5 mGal) extended in the north- western direction 2.5×1.3 km in size, and in magnetic field – in a couple of maximums 500-1000 nTl in amplitude.

Goloskivskiy massif

In this massif of mafic rocks about 90 km2 in size by geophysical data (local gravity maximums about 1 mGal) about 30 minor massifs are distinguished. Some anomalies are proven by drill-holes of deep geochemistry where mafic rocks are intersected. Prospecting works for apatite continue in the given field. To date, Goloskivskiy massif is studied by the structure-prospecting drilling in the north-western part. The field of mafic rocks is located within Khmelnytska fault zone which crosses over here the northern part of Medzhybizkiy enderbite-gneiss dome. In the authors’ mind, in the dome the enderbites of Paleo-Archean Gayvoronskiy complex are exposed at the surface, which contain the remnants of Tyvrivska sequence mafic gneisses. This is the place where Paleo-Archean rocks underwent the least (in relation to remaining field) influence of Neo-Archean and Paleo-Proterozoic granitization processes, that is, the rock associations in general are least enriched in alkalies. Perhaps, these features have caused lack of typical intrusive alkaline rocks in the given field, if one can assume that alkalies are extracted by basaltoid magma from the host rocks. Goloskivskiy massif is located to the west from the same-named village. By drilling data and detailed geophysical works the massif is arc-shaped in the plane and cup-shaped in the cross-section and is extended over 1.4 km being 130-350 m wide. To the depth it is traced by 150 m. Apatite occurrences is discovered in the course of previous works devoted to the field preparation for geological mapping in the scale 1:50 000 [23]. The apatite-biotite gabbro-norite – norite rocks predominate in the central part of the massif. Macroscopically these are dark-grey to almost black, mainly medium-grained, massive or slightly gneiss-like rocks. Amount and relations of opaque minerals – orthopyroxene, clinopyroxene and probably late biotite, are variable. The rocks are mainly mesocratic (40-55% of opaque minerals), medium-grained, in some places more leucocratic (about 30% of opaque minerals) and coarser-grained, rarely – melanocratic (up to 60-65% of opaque minerals). Apatite is permanently contained in the rock in amounts 5-8%, somewhere up to 10%. Apatite content is not changed with the change of opaque minerals content. By the grain shape and mode (inclusions in other rock-forming minerals) apatite looks like one of the earliest minerals. The far southern part of the massif is mainly composed of melanocratic gabbroids, which in places are substituted by pyroxenites. Characteristically, pyroxenes are replaced not only by biotite, as in the central part of the massif, but also by amphibole; the higher apatite content (at the level 7-10% in average) is also noted. The sites are known with both lower (about 5%) and higher (up to 25-30%) apatite content. The latter are encountered in orthopyroxenite, which, apparently, had primarily comprised apatite-pyroxene (perhaps, with olivine) cumulate. In the endo-contact the fine-grained gabbro with quartz (5-10%) is developed. In the exo-contact the quartz-feldspar biotite-hypersthene-garnet metasomatite is described. From the north the massif is limited by the tectonic breaks of sub-latitudinal direction, which are accompanied by tectonic breccia composed of the fragments of clinopyroxene gabbro and quartz-feldspar garnet- bearing (7-8%) rock, similar to the aforementioned exo-contact metasomatite, in cataclazed dark mass. This rock composition and elements of the massif structure allow their consideration as the differentiated gabbroid intrusion which underwent magmatogenic auto-metasomatism. In the rocks of massif’s envelope a range of minor gabbroid, rarely pyroxenite bodies are encountered, which are apparently connected with the massif by the common feeding channel. Gabbro, gabbro-norites, sub-alkaline norites (ν,ενPR1pr), developed in the central part of Goloskivskiy massif, comprise irregular in composition and structure rocks, from leucocratic coarse-grained and pegmatoid to

72 fine-medium-grained melanocratic. Structure is massive, in places banded and pegmatoid. Texture is hypidiomorphic to granoblastic. Major rock-forming minerals are pyroxenes, specifically, hypersthene which often predominates over clinopyroxene (salite-augite). Orthopyroxene content varies from 5-10 to 20-25%, clinopyroxene – up to 20%, often is absent. The total pyroxene content does not exceed 30-35%. Whether clinopyroxene is primary or newly-formed (re-crystallized) mineral is not completely clear. Essential number of pyroxene is replaced by biotite which is contained in amount of 15-30%, somewhere up to 40-50%. Plagioclase (from 20 to 70%) comprises andesine-labrador and also oligoclase- andesine is noted. In the coarser plagioclase grains the antiperthite orthoclase ingrowths are developed. Apatite (5-10%) is normally contained as the inclusions in other rock-forming minerals, the fine elongated (extension 2- 3) crystals 0.1-0.2 mm across. Melanocratic gabbro with plagioclase content 10-25% predominates in the marginal part of Goloskivskiy massif [51]. Texture is hypidiomorphic to granoblastic and lepido-granoblastic. Structure is massive, taxite to stream-like. The rock-forming minerals are distributed more or less uniformly or irregularly, in the zones, enriched in specific mineral. Plagioclase is distributed mainly uniformly, in places its chains are observed, oriented in certain direction. Grain size is commonly 0.5-0.7 mm, rarely granulated grains up to 2-3 mm are developed. The poly- synthetic twinning, often broken, is characteristic. Opaque minerals are irregularly distributed. Among pyroxenes, clinopyroxene commonly predominates. Pyroxenes are replaced by amphibole and biotite in various extents. Essentially pyroxene varieties are noted with insufficient amphibole replacement and stream-like biotite zones, as well as essentially biotite varieties with pyroxene relicts both in amphibole and biotite. Apparently, the processes of pyroxene replacement by amphibole and biotite are slightly split in time. Amphibole (up to 25-30%) is distinct in pleochroism from colorless and olive-green to brown-green. The brown-green coloring is more frequent, characteristic for the high-temperature titanium varieties. Biotite constitutes from 10 to 30-35% of the rock, and apatite – up to 10%. Average chemical composition of major rock varieties of Goloskivskiy massif are given in Table 3.4. Pyroxenites (υPR1pr) comprise plagioclase-bearing, dark-grey, greenish-grey, medium-grained rocks with spotty, stream-like structure. Texture is granoblastic, allotriomorphic, grano-lepidoblastic. Pyroxene (up to 50%) is mainly clinopyroxene which is replaced by amphibole and biotite. Pyroxene and pyroxene-amphibole zones are cut by the mica zones. Pyroxenes comprise isometric, often rounded grains 0.2-0.6 mm in size. Amphibole granoblasts are isometric, often irregular in shape, 0.5-1 mm in size. Plagioclase grains are 0.3-0.5 mm in size, xenomorphic in relation to the opaque minerals. Apatite (5-10%, up to 25-30% in amphibolized, partly biotitized orthopyroxenites) is observed in elongated crystals mainly 0.1-0.2 mm across, located in inclusions in the rock-forming opaque minerals, or in between the latter. Chemical composition of opaque minerals in the mentioned gabbroid varieties is given in Table 3.5. By the chemistry (see Table 3.4) the mafic rocks of Goloskivskiy massif exhibit increased alkalinity (K2O+Na2O = 5-6%) and are most closer to orthoclase gabbro and by this parameter they strongly differ from the rocks of Sabarivskiy complex. The mafic rocks (gabbro, gabbro-norites, norites) display high values of density: in 95% of measured samples the average density is 2.90 g/cm3 with the range from 2.80 to 3.12 g/cm3. By magnetic properties these rocks are more uniform: 70% of samples exhibit magnetic susceptibility values from 50 to 300×4π×10-6 CI units, -6 and 20% of samples are high-magnetic with æavg. = 500÷4554×4π×10 CI units. Average value of magnetic susceptibility in gabbro, gabbro-norites and norites is 356×4π×10-6 CI units. The average value of residual -3 -3 magnetization Iravg. = 307×10 A/m, although in 80% of samples Ir does not exceed 70×10 A/m. Pyroxenites, gabbro-pyroxenites are higher in density (average value is 3.07 g/cm3 with the range for 95% of samples from 2.97 to 3.19 g/cm3), magnetic susceptibility (average value is 1626×4π×10-6 CI units with the range for 60% of samples from 200 to 12642×4π×10-6 CI units) and residual magnetization (average value is 645×10-3 A/m with variations from 1 to 48124×10-3 A/m). After results of detailed gravity-magnetic surveys in the scale 1:10 000 in Goloskivska site the massifs of mafic rocks are expressed in the local small-size (from 300×300 m to 500×800 m) gravity maximums with amplitude 0.4-0.8 mGal. In the intricate magnetic field created by charnockitoids and high-magnetic mafic gneisses, they are expressed in the areas of gentle Ta field, relative minimums and, in some cases, in the magnetic anomalies up to first hundreds of nTl in amplitude, coinciding with the gravity maximums. Thus, the rocks of Proskurivskiy complex are arranged in the typical for the alkaline-gabbroid formation natural tange: gabbro – essexites – ijolites – nepheline syenites – alkaline syenites – syenites – quartz syenites – phenites.

73 The unity of this range is clearly expressed in the positive geochemical specialization all, without exceptions, rocks in the complex for phosphorus, barium, manganese, strontium, chromium, vanadium, titanium, yttrium, ytterbium, and negative specialization for lithium, lanthanum, germanium, as well as silver, lead, and molybdenum.

Table 3.4. Average chemical composition (%) of major rock varieties in Goloskivskiy massif

Melanocratic gabbro vPR pr Gabbro-norite vPR pr Oxides, ratios 1 1 (n=56) (n=61) SiO2 42.82 49.52 TiO2 1.36 0.98 Al2O3 10.70 16.44 Cr2O3 0.05 0.042 V2O3 0.02 0.02 Fe2O3 3.42 2.32 FeO 6.72 4.28 MnO 0.15 0.10 MgO 13.90 8.29 CaO 10.33 7.57 Na2O 1.43 3.18 K2O 2.59 2.55 P2O5 3.46 2.38 SO3 0.37 0.30 CO2 0.18 0.10 F - - + H2O 1.48 0.94 - H2O 0.20 0.20 Sum 99.18 99.21 Na2O+K2O 4.02 5.73 Na2O/K2O 0.55 1.24

With the given complex are occurrences and point of increased apatite mineralization, first of all, the high-perspective Goloskivskiy occurrence in gabbroids, Verbkivskiy – in shonkinites; occurrences, points of increased mineralization and geochemical anomalies of rare earths, geochemical anomalies of titanium, zirconium, barium, strontium, as well as chromium, nickel, and vanadium.

Table 3.5. Chemical composition (%) of opaque minerals in the major rock varieties of Goloskivskiy massif

Pyroxene Amphibole Biotite Oxide Melanocratic Gabbro- Melanocratic Melanocratic Gabbro- Pyroxenite Pyroxenite gabbro norite gabbro gabbro norite SiO2 53.494 52.831 52.98 44.462 45.04 40.725 40.84 TiO2 0.063 0.104 0.11 1.18 1.12 2.213 2.42 Al2O3 1.197 0.683 0.76 10.695 10.68 11.614 12.06 Cr2O3 - - - 0.023 - 0.161 0.20 FeO 20.784 25.754 24.52 10.361 10.82 7.375 8.02 MnO 0.499 0.599 0.50 0.164 0.22 - 0.12 MgO 22.900 19.524 20.44 14.114 14.86 21.199 22.40 CaO 0.521 0.520 0.50 12.095 12.40 0.028 0.05 Na2O 0.016 - - 1.741 1.68 0.177 0.54 K2O 0.003 - 0.002 1.186 1.26 9.752 9.68 Sum 99.441 99.975 99.812 96.021 98.08 93.244 96.33

74 The age of zircons from sub-alkaline gabbro of Goloskivska site is 2053+13 Ma, from Verbkivskiy shonkinite – 2024+61 Ma (Table 3.6). Considerable error in the second case is related to the lack of the zircon points’ extension along discordia. However, since obtained data are overlapping, with necessary confidence these rocks can be considered coeval, formed within the time interval 2050-2060 Ma. These absolute age data are supplementary for the inclusion of the alkaline mafic rocks and mafic gabbro with slightly increased alkalinity to the single complex.

Table 3.6. Results of isotopic-geochronological studies of zircons from Verbkivska and Goloskivska sites

Ppm Isotopic ratios Zircon fraction U Pb 206Pb/204Pb 206Pb/207Pb 206Pb/208Pb Shonkinite of Verbkivska site (1585/13) I e/m 2007 729 1983 7.7345 5.1709 II e/m 194 71 1631 7.6177 4.7433 n/m 70 28 2514 7.7487 4.7782 Not separated 1957 738 2771 7.7887 4.3835 Sub-alkaline gabbro of Goloskivska site (1587/12) n/m, <0.05 69 27.5 6667 7.7719 8.6080 e/m, >0.05 844 315 3299 7.5948 6.5598 n/m, >0.05 560 213 4097 7.6895 8.1007 Not separated 730 293 5498 7.7291 6.7616

Isotopic ratios Age, Ma Zircon fraction 206 238 206 235 206 238 206 235 206 207 Pbr/ U Pbr/ U Pbr/ U Pbr/ U Pb/ Pb Shonkinite of Verbkivska site (1585/13) I e/m 0.31649 5.3547 1773 1878 1996 II e/m 0.31403 5.3365 1761 1875 2004 n/m 0.34256 5.8517 1899 1954 2013 Not separated 0.32125 5.4802 1796 1898 2011 Sub-alkaline gabbro of Goloskivska site (1587/12) n/m, <0.05 0.37248 6.5126 2041 2048 2054 e/m, >0.05 0.33605 5.9214 1868 1964 2068 n/m, >0.05 0.35092 6.1426 1939 1996 2056 Not separated 0.36443 6.3869 2003 2031 2058

Notes: r – radiogenic Pb, n/m – non-magnetic fraction, e/m – magnetic fraction.

Zhdanivska association of ultramafic rocks (PR1žd)

For the first time Zhdanivskiy intrusive massif, located in 200 m to the south-east from Zhdanivka village, Khmelnytskiy area of Vinnytska Oblast, was discovered in the course of prospecting works for diamonds in 2003. Magnetic anomaly was encountered by results of analysis and re-interpretation of Za field at the level of primary digital data of magnetic survey in the scale 1:25 000.

Taking into account the field mapping results, Zhdanivska structure is expressed in magnetic field Ta with the maximum about 400 nTl in amplitude, elliptic in shape 270×60 m in size, the long axis is oriented in the north-western direction (azimuth 325o). By the results of the 3D magnetic field modeling, Zhdanivska structure looks like overturned irregular cone which top goes into the central “leg” of sub-vertical dipping and “indefinite”, in geophysical sense, extension to the depth. In the regional gravity field Zhdanivska site is located in the zone of northern exo-contact of Khmilnytskiy minimum ga, caused by intrusion of the same-named granitoids. Within magnetic anomaly, according to the gravity survey data in the scale 1:5 000, Zhdanivska structure coincides with the local gravity minimum 0.3 mGal in amplitude. In 2004, in the course of EGSF-200, aiming adjustment of tectonic position, structure, petrology and metallogeny of Zhdanivskiy massif, the profile was drilled consisting of three structure-mapping boreholes: two inclined and one vertical (Fig. 3.1), where occurrence of the ultramafic rock massif was proven. All drill-holes

75 have intersected host rocks composed of garnet-biotite granites, migmatites and plagio-migmatites of Berdychivskiy complex with xenoliths of garnet-biotite gneisses of Bereznynska sequence. The magma feeding channel, excepted by the results of geophysical modeling, is not identified. Thus, from the total amount of data available, the massif is asymmetric-cone with the steeper eastern contact. The maximum identified vertical thickness is 170.0 m.

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Ultra-metamorphic and intrusive rocks: Berdychivskiy complex (PR1bd): 1 – garnet-biotite plagiogranites (ργ) and plagio-migmatites (ργm); 2 – garnet-biotite granites (γ) and migmatites (γm); Zhdanivska rock association (PR1žd): 3 – pyroxenites (υ); 4 – peridotites (υσ). Metasomatic alteration of crystalline rocks: 5 – albitization (al); 6 – weathering crust of crystalline rocks. Sedimentary rocks: 7 – clays; 8 – loams; 9 – sands; 10 – drill-holes (49- drill-hole number, depth); 11 – tectonic breaks.

In the tectonic respect the massif is located at the cross-junction between three diverse-oriented fault zones: the north-western (Khmilnytska), sub-longitudinal (Bilokorovytsko-Yablunivska), and sub-latitudinal. The fresh (not altered by secondary processes) rocks of the massif exhibit the typical igneous (panidiomorphic and gabbroic) textures. Intrusion, in our mind, is hidden-layered with more mafic central part, consisting of apo- peridotites, and marginal parts, mainly composed of pyroxenites (υσ, υPR1žd(?)). The column of Zhdanivska intrusion by drill-hole 49 is as follows:

Rock name Depth, m Thickness, m Serpentinite (apo-peridotite). Extensively altered ultramafic rock composed of magnetite – 35-40%, biotite – 30-35%, serpentine 1. (bastite) – 25-30%. Rock texture is metasomatic to sideronitic in 61.0-67.5 6.5 places of magnetite accumulation. The rock is resulted from the secondary alteration in the supergene zone. Cataclasite after granite. Mineral composition: plagioclase+quartz – 2. 80%, biotite – 20%. Rock texture is cataclastic. Extensive 67.5-67.7 0.2 granulation of the leucocratic portion is observed, biotite is hydrated Peridotite, extensively altered by epigenetic processes, in composition – harzburgite. Texture: primary is not identified, secondary – loopy haphazard. Mineral composition: olivine – 70% 3. (replaced by serpentine-chrysotile); orthopyroxene – 20%; 67.7-103.4 35.7 clinopyroxene – 5%, carbonate – 5%. Ore mineral: magnetite (secondary). The rocks is cut by numerous carbonate veinlets from tenth to 2.0 mm, diverse-oriented Olivine orthopyroxenite. Texture is panidiomorphic. Mineral 4. 103.4-107.7 4.3 composition: orthopyroxene (bronzite) – 85%, olivine – 15% Norite. Texture is gabbroic (panallotriomorphic). Mineral 5. composition: orthopyroxene – 60%, clinopyroxene – 5%, plagioclase 107.7-114.4 6.7 (labrador) – 35% Orthopyroxenite. Texture is panidiomorphic and gabbroic. Mineral 6. composition: orthopyroxene – 85%, clinopyroxene – 5%, plagioclase 114.4-118.8 4.4 (labrador) – 10% Cataclazed plagiomigmatite with veins of pink-grey aplite- pegmatoid granites and gabbro xenoliths up to 20-30 cm. At the top of run the rock is extensively biotitized. Texture is lepidoblastic, 7. 118.8-125.5 6.7 lepido-granoblastic. Mineral composition: plagioclase – 55-60%, quartz – up to 25%, biotite – 15-20%; at the depth 118.8-122.1 – up to 93% Garnet-biotite pink-grey migmatite. Texture: granoblastic, lepido- granoblastic. Mineral composition: plagioclase (oligoclase-andesine) 8. – 40-45%, K-feldspar-perthite – 15-30%, quartz – 15-35%, garnet – 125.5-190.5 65.0 up to 10%. Accessories: apatite, zircon, monazite. Ore minerals: magnetite, sulphides

Structure of the massif, described above, is also similar in the columns obtained by other structure- mapping drill-holes. The contact of massif with plagio-migmatites and migmatites in DH 49 is tectonic, with notable processes of superimposed biotitization and sulphidization. In DH 50 the contact between orthopyroxenites and Berdychivski melanocratic plagio-migmatites is very sharp, clear, under the angle 20-25o to the core axis. The chilling zone is not observed. Additional criteria for the confidence of inter-hole correlation include study results of the dipping elements by method of electric correlation in the inter-hole and hole-surface versions. Under the total majority of data it can be concluded that the western and eastern limbs of studied geological structure have different rock dipping angles. Apparently it is related to the tectonic activity (faults) identified in DH 50 by the resistance logging data. Thus, mentioned contact relations do not provide unequivocal information on the relationships between the massif rocks and its surroundings. Granitoid enclaves in ultramafic rocks established in the core (DH 49, depth 67.5-67.7 m; DH 50, depth 96.3-97.2 m) comprise the fragments of cataclazed rock and it is not possible to define precisely whether these are tectonised granite injections or, conversely, granite xenoliths. Occurrence of melanocratic plagio-migmatites at the massif exo-contact, which are gradually substituted by mesocratic two- feldspar migmatites, can be explained either by the process of ultramafic rocks granitization or by the granitoid basification during emplacement of ultramafic intrusion. Specific attention to Zhdanivska intrusion was paid because of uranium occurrence discovered in the course of prospecting for diamonds and increased concentrations of platinoids and gold. After the gamma-

77 logging data the anomaly of natural gamma-radiation has been established. The lower by intensity of radiation zones were also identified in DH 49. After results of mineralogical studies high enough uranium content is supported by occurrence of uraninite and uranium black in metasomatically altered rock at the massif endo-contact, and increased platinoid content – by sperilite finding. From results of emission quantometric express-analysis for platinoids, conducted by S.E.Popovchenko in the National Mining University (Dnipropetrovsk town), the maximum platinum content does nor exceed 0.11 g/t, Pd – up to 1.2 g/t, Ru – up to 1.09 g/t, and gold – up to 0.26 g/t; coupled with insufficient massif size (see above) this does not allow its positive assessment in tern of precious metals. Aiming the absolute age determination in the rocks of Zhdanivskiy massif 6 samples of altered peridotites and pyroxenites 10-12 kg in weight each were taken from drill-holes and transferred to IGMOF UNAS. Unfortunately, neither U-Pb nor K-Ar methods were able to determine the rock age because of zircon and primary amphibole lacking in the rock. The model age, determined by Sm-Nd method, is 1856-1862 Ma (IGMOS UNAS, L.V.Shumlyanskiy), and this provided the ground to distinguish these rocks in the separate association and put it in the legend at the mentioned age level. However, the issue of the age and complex affinity of Zhdanivski massif rocks requires further studies. The rocks of Zhdanivska association in composition are close enough to the rocks of Kapitanivsko- Derenyukhivskiy and Sabarivskiy complexes. By SiO2 content the mafic-ultramafic rocks of Zhdanivska intrusion (39.1-48.82%) do correspond to the majority of ultramafic rocks developed in Middle and Upper Pobuzhzhya but essentially differ by other major elements. The alumina contents (3.36-7.49%) and Na2O+K2O (0.49-1.31%) are more similar to the contents of these oxides in the rocks of Sabarivskiy complex (Al2O3 – 9.43%, Na2O+K2O = 1.77%) and considerably differ from the rocks of Kapitanivsko-Derenyukhivskiy complex 1 (Al2O3 – 1.82-1.05%, Na2O+K2O = 0.17%)0 . By MgO content Zhdanivski ultramafic rocks (11.54-24.58%) are also similar to Sabarivski ones (18.58%) and differ from Kapitanivsko-Derenyukhivski (22.89-40.95%). The same relations are observed for CaO (6.89-8.11% for Zhdanivski; 9.94% for Sabarivski; 2.58-2.70% for Kapitanivsko-Derenyukhivski rocks). By alkali content Zhdanivski rocks considerably differ from the mafic- ultramafic rocks of Bukynskiy (Na2O+K2O = 5.7%) and Proskurivskiy (Na2O+K2O = 3.7%) complexes. By the average content of siderophile (Cr, Ni, Co) micro-elements the rocks of Zhdanivska intrusion differ from Kapitanivsko-Derenyukhivski ones in the lower values: Cr – 0.10% against 0.23-1.10%; Ni – 0.10% against 0.10-0.29%. At the same time, siderophile content is much higher than in the rocks of Proskurivskiy and Bukynskiy complexes: Cr – 0.10% against 0.008% (Bukynskiy) and 0.01 (Proskurivskiy); Ni – 0.10 against 0.003% (Bukynskiy) and 0.006% (Proskurivskiy). Over some intervals in Zhdanivskiy massif contents of chromium is 0.5% and nickel 0.3-0.5% and these are much lower than in the rocks of Kapitanivsko-Derenyukhivskiy complex, enriched in these elements, and similar to the rocks of Sabarivskiy complex. Thus, by chemistry the rocks of Zhdanivska intrusion are closest to the rocks of Sabarivskiy complex developed in Upper and Middle Pobuzhzhya, suggesting one more time for the needs in detailed studies of the age of their formation.

Dyke complex (PR1)

In the studied area the dyke rocks of mafic composition – diabase and gabbro-diabase dykes (β,vPR1) 3 are mapped. They exhibit high values of density (σavg. = 3.10 g/cm), magnetic susceptibility (æavg. = -6 -3 2700×4π×10 CI units), and residual magnetization (Ir = 310×10 A/m). In the magnetic field diabases are expressed in the chain of minor linear anomalies 30-40 nTl in amplitude. In the gravity field they are not reflected because of small size but in case of available gradient measurement they correspond to the positive anomalies Vxz. By geophysical data the chains of diabase dykes are observed in the arc over the distance of 22 km (the south-eastern part of the map sheet) and are confined to the most weakened tectonic zones. At the surface the dykes are exposed in the western outskirt of Guli village, and are intersected in the quarry of Shyroka Greblya village and by numerous drill-holes [24, 26, 47]. Their thickness attains 4 m. The dykes are mainly conformable to the host rock banding and gneissosity, under various azimuths (from 90 to 340o) and angles (from 40 to 85o), and follow specific tectonic breaks. The dykes are most widespread in the zone of Khmilnytskiy fault. The composition of dykes and their occurrence in the fault zone with peak activity in Paleo-Proterozoic allow their correlation with the formation of the dyke complex of this age (~1600 Ma) [10] according to the valid

1 Hereafter chemical parameters are given after I.B.Shcherbakov [9] for Kapitanivsko-Derenyukhivskiy complex and after A.S.Voynovskiy [18] for Proskurivskiy and Bukynskiy complexes.

78 chrono-stratigraphic scheme. The dykes are cut by tectonic fractures although the rocks did not undergo significant alteration. Diabases are the dark-grey to black, medium-, rarely fine-grained rocks with massive structure. Under microscope texture is disbasic (ophitic). Mineral composition: plagioclase – 50-60%, clinopyroxene – 5-15%, orthopyroxene – up to 10%, olivine – 5%, biotite – up to 5%, potassium feldspar – 2- 3%, ilmenite – up to 5%. Plagioclase commonly is labrador-andesine (No. 45-50). Grain shape is lath-like 2-4 mm long and 0.2- 0.6 mm wide. Some plagioclase grains are tabular (in those rock varieties where potassium feldspar is developed). Plagioclase is twinned under complex rule: albite in combination with Karlsbadian. Often plagioclase replacement by potassium feldspar is observed. In cataclased varieties of diabases plagioclase laths are turned and folded, the wavy extinction is noted. Olivine (ironiferous fayalite) in thin sections is colorless, macroscopically – light-yellow-green. Grain shape is tabular. Most olivine grains contain ore mineral inclusions. Olivine grains are surrounded by the narrow (~0.05 mm) hypersthene rim. Orthopyroxene (hypersthene) is observed in druzite after olivine. Clinopyroxene (augite) is developed in small elongated tables, in thin sections slightly predominates over hypersthene and is irregularly brownish-pink-colored. Around augite grains the narrow rim of green amphibole is noted, which in turn is substituted by biotite, in places chlorite. Biotite in thin section is reddish- brown and surrounds ore mineral grains. The rock texture, composition and minerals suggest for the formation under hypabyssal conditions. It is also supported by petrochemical features. Average chemical composition is as follows: SiO2 – 49.12%, Al2O3 – 16.85%, Fe2O3 – 9.84%, FeO – 6.47%, TiO2 – 1.14%, MnO – 0.14%, CaO – 4.5%, MgO – 5.35%, P2O5 – 0.90%, K2O – 1.8%, Na2O – 2.23%. By the high enough sum of alkali and lower silica contents they belong to the mafic rocks of sub- alkaline range. By the spectral analysis data, the high phosphorus – up to 0.7-1.0% and lithium – up to 10×10-3% is noted, and very low, as for the mafic rocks, siderophile-group element contents: Cr – up to 10×10-3%, Ni – up to 10×10-3%, Co – 7×10-3%.

25Ultra-metamorphic rocks

63Archean Eon

106Paleo-Archean Era

Podilska LTZ

Gayvoronskiy complex (enAR1gv(?))

Enderbites of Gayvoronskiy complex are exposed at the surface in Medzhybizkiy dome (exposed in Rusanivskiy quarry) and intersected by single mapping and structure-prospecting drill-holes 1803-1806 [51] in the southern part of map sheet. By composition enderbites or enderbite-migmatites (enAR1gv(?)) are tonalites or diorites with banded structure. The authors follow an idea that the rocks of Gayvoronskiy complex have been formed in the course of 1 the oldest (3.4 Ga after M.P.Shcherbak [10]1 ) granitization stage resulted in the continental-type proto-crust development. In the opinion of many authors, the substratum for the complex had included the rocks of Dnistersko-Buzka Series, mainly pyroxene mafic gneisses, and the mafic-ultramafic rocks of Sabarivskiy complex. Over most part of the territory due to the later-stage granitization (Meso-Archean and Paleo- Proterozoic) these rocks underwent remobilization and re-crystallization with complete or significant loss of evidences for the affinity to this complex and development of new rock associations.

1 The age of 3.4 Ga is established for the early generation of zircons. At the same time, these rocks also contain the younger zircon generation (2.8-2.9 Ga), and therefore, the issue of Gayvoronskiy complex definition is disputable – Ed.

79 Enderbites are grey, mainly medium-grained rocks, slightly-banded or massive, with elements of gneissosity. Under microscope: texture is granoblastic, hetero-granoblastic; mineral composition: plagioclase – 50-70%, orthopyroxene (hypersthene) – 5-10%, clinopyroxene is commonly lacking although somewhere diopside is noted in amount up to 1%. Biotite is also developed in some places in amount up to 5%. Quartz constitutes 20-25% of rock in average but in melanocratic varieties its amount decreases to 5-10%, and in leucocratic ones increases to 35%. Plagioclase is oligoclase-andesine, hypersthene with slight pleochroism, high- ironiferous enough. Accessory and ore minerals are contained in minor amounts, normally these are apatite and magnetite. By petrochemical parameters (average content in %): SiO2 – 64.85, TiO2 – 0.48, Al2O3 – 14.74, Fe2O3 – 2.49, FeO – 3.69, MnO – 0.10, MgO – 2.49, CaO – 4.0, Na2O – 3.88, K2O – 1.52, P2O5 – 0.11, and ratio K2O/Na2O = 0.39, the enderbites correspond to tonalites or diorites. The rocks of Gayvoronski complex do not display any clear geochemical specialization for micro- elements but their slight positive specialization for barium, nickel, chromium, molybdenum, zirconium, and negative for yttrium, silver, and lithium should be noted. Gneiss-like enderbites exhibit steady increased values of density from 2.7 to 2.91 g/cm3 (2.80 g/cm3 in average) with wide variability range of magnetic susceptibility: 50% of samples are low-magnetic (modal value -6 -6 æavg. = 50×4π×10 CI units), 30% are magnetic (modal value æavg. = 200×4π×10 CI units), and 20% are high- -6 -6 magnetic (æavg. = 2000×4π×10 CI units). The high values of magnetic susceptibility (æavg. = 779×4π×10 CI -3 units), and also residual magnetization (Ir = 461×10 A/m) are characteristic for the samples of so called enderbite-gneisses (granitized in various extents Tyvrivska sequence mafic gneisses of Dnistersko-Buzka Series) collected from structure-prospecting drill-holes. By the columns of these drill-holes the change is observed from hypersthene and two-pyroxene mafic gneisses through enderbitized gneisses and mafic gneisses to enderbite- gneisses and enderbites. The density and magnetic susceptibility of the rocks depend on the degree of substratum granitization. The fields of Gayvoronskiy complex enderbites are expressed as the areas of increased values of magnetic field with mosaic patterns and intensity up to hundred nTl and more, which coincide with the positive low-amplitude local gravity anomalies.

107Meso-Archean Era

Litynskiy complex (AR2lt)

The rocks of Litynskiy ultra-metamorphic complex are developed over entire territory of the map sheet, except its far north-western part (Volynskiy mega-block), and occupies about 10% of the area. Litynskiy complex includes: charnockites and pegmatoid charnockites, massive coarse-medium- grained, mainly leucocratic enderbites, as well as fine-medium-grained, often shadow, enderbite-migmatites. Enderbites and charnockites are most developed in Litynskiy, Medzhybizkiy and Starokostyantynivskiy blocks. Enderbites of Gayvoronskiy and Litynskiy complexes somewhat differ one from another by mineral and chemical composition but are very similar visually and in their relations with the rocks of Dnistersko-Buzka Series. It should be noted that other members of charnockitoid association are younger in comparison to enderbites. Available marker dating in 2.8 Ga, after I.M.Lesnaya [4], for melanocratic enderbite-migmatites and massive leucocratic enderbites, in spite of insufficient isotope age reduction by relations 207Pb/205Pb, precludes their separation into different complexes. That is, in this case enderbite-migmatites can be considered as Paleo- Archean rocks remobilized at the boundary between Meso- and Neo-Archean, whereas massive leucocratic enderbites – as the products of further granitization and re-crystallization. Charnockites and pegmatoid charnockites (čAR2lt). Charnockites of Litynskiy complex comprise the final product of Meso-Archean granitization over Paleo-Archean rock substratum that had been formed under essential potassium activity under conditions of granulite facies metamorphism. In contrast to enderbites spatially related to the dome structures, charnockites are confined to the inter- dome areas and in the domes are developed in the weakened extension zones. Major substratum for charnockites had included migmatite-enderbites and all other enderbite varieties, rarely the rocks of Dnistersko-Buzka Series. The natural outcrops of charnockites are not known in the studied map sheet and they are only intersected by the mapping drill-holes [47, 51]. Under charnockitization of enderbite-migmatites, gneiss-like enderbites, gneisses and mafic gneisses the shadow, rarely unclear-banded meso- and melanocratic rocks are developed composed of plagioclase-antiperthite – 25-35%, K-feldspar-perthite – 25-30%, quartz – 10-15%, hypersthene – 10-15%. Biotite (up to 7%) is

80 developed after hypersthene. Of the ore minerals, magnetite and ilmenite are observed. After leucocratic enderbites the massive medium-coarse-grained charnockites are developed with K-feldspar content up to 50%, plagioclase – 25-40%, quartz – up to 25%, hypersthene – 5-8%, biotite – 5-7%. Of the ore minerals, magnetite is most frequently observed. Somewhere in charnockitoids, rarely their hosting gneisses, the bodies up to 3 m thick of pegmatite- charnockites are observed. Their composition: K-feldspar-perthite – 60-80%, plagioclase – 10-15%, quartz – up to 10%, hypersthene – 5-8%. Of accessories, apatite, zircon and magnetite are observed. Average chemical composition of Litynskiy complex charnockites (%): SiO2 – 65.51, TiO2 – 0.47, Al2O3 – 15.65, Fe2O3 – 2.64, FeO – 1.99, MnO – 0.14, MgO – 1.84, CaO – 3.10, Na2O – 3.30, K2O – 3.67, P2O5 – 0.07. By the micro-element content, charnockites contain increased concentrations of zirconium, niobium and molybdenum; their negative specialization is for vanadium and lithium. Massive leucocratic enderbites (enAR2lt). As noted above, enderbites are developed in the enderbite- charnockite domes and are encountered in the area of Goloskiv, Lysogirka villages. Leucocratic enderbites constitute the central part of Litynskiy dome where they are associated with leucocratic granulites, and are also developed in Medzhybizkiy dome. Enderbites are studied in the outcrops along Zgar river [51] and intersected by some mapping drill-holes [51]. Enderbites are observed in the band-like intercalation with mainly two- pyroxene mafic gneisses. The contact relations are mainly gradual. Massive leuco-enderbites are light-grey medium-coarse-grained rocks with distinct bluish quartz. Under microscope texture is blasto-granitic, hypidiomorphic, anti-perthitic with elements of myrmekite, structure is massive. Major rock-forming assemblage: hypersthene (8-15%) + plagioclase (anti-perthite) (60%) + quartz (15- 25%). Clinopyroxenes are not characteristic. Biotite and potassium feldspar (up to 5-8%) are observed. Chemical composition of enderbites is given in Table 3.7.

Table 3.7. Chemical composition of enderbites of Litynskiy complex

Oxides, ratios X, % Min Max SiO2 73.57 71.92 75.21 TiO2 0.16 0.10 0.21 Al2O3 14.63 13.20 16.06 Fe2O3 0.03 0.02 0.03 FeO 1.28 1.23 1.33 MnO 0.25 0.20 0.30 MgO 0.45 0.28 0.61 CaO 1.78 1.33 2.23 Na2O 3.21 2.62 3.79 K2O 3.96 3.27 4.64 - H2O 0.20 0.20 0.20 + H2O - - - P2O5 0.05 0.05 0.05 SO3 0.09 0.04 0.13 Ssulf. - - - CO2 - - - LOI 0.41 0.37 0.44 Sum 100.03 99.97 100.09 3 3 3 V3 5.4×10 3.2×10 12.2×10 V4 59.62 41.5 97.7 Na2O+K2O 7.16 7.06 7.26 Na2O/K2O 0.81 0.56 1.16

Note: see Table 3.1 and 3.2 for the meanings of petrochemical coefficients.

Hypersthene is observed in prismatic and tabular grains with notable pleochroism, MgO content is high (up to 18%). Plagioclase, like enderbite-migmatites, is mainly oligoclase with abundant anti-perthite ingrowths. Biotite is red-brown.

81 Leucocratic enderbites in the plot SiO2 – (Na2O+K2O) fall into the field of low-alkali granites. It should be noted that by ratio Na2O/K2O (for leucocratic enderbites – 0.81) and SiO2 content one may conclude that leucocratic enderbites have been formed under increased silica and potassium activity. Leucocratic enderbites exhibit positive specialization for phosphorus, lanthanum, cerium, barium, and negative – for manganese, strontium, vanadium, titanium, nickel, yttrium, and ytterbium. It should be noted that in leucocratic enderbites, in comparison with enderbite-migmatites of Gayvoronskiy complex, concentration coefficients of siderophyle-group elements are lesser: Cr – 0.6 against 0.9, Ni – 0.5 against 0.6, Co – 0.7 against 0.8, V – 0.4 against 0.6, that probably indicate the tighter link of enderbite-migmatites with the substratum rocks. By physical properties the rocks of Litynskiy complex considerably differ one from another. 3 Charnockites are steady in term of density (σavg. = 2.69 g/cm ) and wide range of magnetic susceptibility -6 – from actually non-magnetic to magnetic and high-magnetic (æavg. = 731×4π×10 CI units) [51]. Residual magnetization is also increased, being 709×10-3 A/m in average. In the north-eastern part of map sheet the pyroxene-biotite charnockites and amphibole-pyroxene-biotite charnockites of granodiorite composition are distinguished [15]. By the magnetic and density properties these -6 -3 rocks are divided in 3 groups: non-magnetic (æavg. = 45÷54×4π×10 CI units; Iravg. = 39÷64×10 A/m), low- -6 -3 magnetic (æavg. = 196÷335×4π×10 CI units; Iravg. = 224÷373×10 A/m), and magnetic (æavg. = -6 -3 2990÷3775×4π×10 CI units; Iravg. = 1202÷674×10 A/m). Density of these rocks varies from 2.68 g/cm3 to 2.77 g/cm3. Charnockites are expressed in the positive magnetic fields of mosaic structure (Starokostyantynivskiy massif), or individual isometric or elliptical anomalies from some tens to thousand nTl (for example, Ostropilska, Bychivska, Lysogirska, Skarzhyntsivska, and others), which coincide with the negative local gravity anomalies. 3 Leucocratic (massive) enderbites are relative light rocks (σavg. = 2.73 g/cm), in more melanocratic 3 varieties σavg. = 2.75 g/cm . Their magnetic properties are unsteady: in cases when substratum included low- magnetic hypersthene mafic gneisses and enderbite-migmatites, the rocks are low-magnetic (æavg. = 50÷80×4π×10-6 CI units). At the sites composed of high-magnetic two-pyroxene and hornblende-pyroxene mafic gneisses the rock magnetization attains 1200÷2000×4π×10-6 CI units, maximum – 5000÷7000×4π×10-6 CI units -6 (æavg. = 480×4π×10 CI units). Variability range of residual magnetization is also wide – from 0 to 2000×10-3 A/m, but distribution -3 histogram is single-modal with average value Iravg. = 182×10 A/m. The most magnetic varieties are developed in Litynskiy dome, Medzhybizkiy and Veselivskiy blocks, where they are expressed in the positive magnetic fields of complex mosaic structure from some hundreds to 1000-3000 nTl in some extremes, or in the individual linear or arch-shaped anomalies from tens to hundreds nTl (map sheets M-35-91-A,C).

64Proterozoic Eon

108Paleo-Proterozoic Era

Novograd-Volynska LTZ

Sheremetivskiy complex (PR1šr)

The rocks of Sheremetivskiy complex occupy the far north-western part of map sheet and are intersected by single drill-holes to the north-west from Teterivskiy fault and to the north from Andrushivskiy fault. This complex includes biotite plagio-granites and plagio-migmatites, and amphibole-biotite plagio- migmatites of granodiorite and tonalite composition. These rocks in the studied area are encountered in the course of DGM-200 nearby Grytsiv, Brazhynka villages, and also intersected by drill-holes of the predecessors [20]. In the mentioned areas just the migmatites of diorite composition adjoin Vasylivska Suite rocks of Teterivska Series. Granitoids of Sheremetivskiy complex are intruded by the rocks of Varvarivskiy massif (Bukynskiy complex). Amphibole-biotite plagio-migmatites of tonalite and granodiorite composition (γδPR1šr) are developed in the local bodies up to 400 m thick within amphibole-biotite, biotite gneisses and amphibolites, which contain xenoliths of the latter, that is, tightly associated with them. In the map of gravity field plagio-migmatites are expressed in the positive gravity anomalies from 0.5 to 1.5 mGal. Macroscopically plagio-migmatites are grey, fine-medium-grained rocks, mainly massive, unclear-banded, often with plagioclase porphyry-blasts.

82 Under microscope texture is granoblastic, lepido-granoblastic, in places up to cataclastic granitic, hypidiomorphic; mineral composition: plagioclase, in coarse grains anti-perthite – 70-80%, quartz – up to 24- 30%, biotite – 5-8%, amphibole – up to 8-10%, in places muscovite up to 2%. Accessory minerals: apatite, monazite, garnet, magnetite, ilmenite, pyrite. Plagioclase is commonly sodium (albite-oligoclase), in mafic varieties up to andesine, observed in irregular tabular grains, somewhere with anti-perthite ingrowths. Some crystals contain muscovite flakes. Grain size is from 0.2 to 0.6 mm. Quartz is observed in the grains or allotriomorphic intergrowths, or fills up the space between other minerals, rarely in the inclusions in feldspars. Extinction is wavy. Biotite is developed in the elongated flakes up to 2 cm in size, dark-brown, irregularly distributed in the rock. Muscovite does not provide separate grains and is only observed in the intergrowths with biotite. Amphibole comprises common green hornblende 2-5 mm in size. Apatite fills up the space between other minerals in the rounded or irregular grains up to 0.2 mm in size, mainly colorless. By the petrochemical parameters amphibole-biotite and biotite plagio-migmatites are variable. SiO2 content varies from 60.50 to 69.35% being 65.46% in average; average content of other oxides: TiO2 – 0.43%, Al2O3 – 16.97%, Fe2O3 – 1.65%, FeO – 2.96%, MgO – 2.42%, CaO – 4.44%, Na2O – 3.84%, K2O – 1.28%, Na2O/K2O – 3.0. In migmatites of tonalite and granodiorite composition zirconium, lithium, barium, and cerium are contained in increased amount, whereas chromium, nickel and copper are reduced [17]. Biotite plagio-granites and plagio-migmatites (pγ, pγmPR1šr). Like other rocks of Sheremetivskiy complex, they are observed to the north from Andrushivskiy fault and to the north-west from Teterivskiy fault. The difference between the varieties of this rock group is caused by the substratum (Vasylivska Suite) granitization degree. Plagio-migmatites macroscopically are grey, from fine- to coarse-grained rocks, often with plagioclase porphyry-blasts and banded, shadow, rarely lens-like structure. Plagio-granites are also grey, medium-coarse-grained rocks with massive structure. Texture of plagio-granites is granitic, granoblastic, in places lepido-granoblastic. Mineral composition of plagio-migmatites and plagio-granites: plagioclase (oligoclase-albite) – 50-80%, K-feldspar – up to 10%, quartz – 20-35%, biotite – 2-20%, in places muscovite up to 2%, sillimanite, garnet. Accessories: zircon, monazite. Plagioclase (albite-oligoclase) is observed in prismatic grains with irregular edges, often poly- synthetically twinned or grown by microcline. Quartz fills up the space between biotite and plagioclase crystals, somewhere contains biotite inclusions, and also is observed in inclusions in plagioclase. Biotite is observed in elongated flakes or in the bunch-like aggregates. Chemical composition of plagio-granites and plagio-migmatites (in average): SiO2 – 69.61%, TiO2 – 0.27%, Al2O3 – 15.65%, Fe2O3 – 0.83%, FeO – 2.24%, MnO – 0.035%, MgO – 1.37%, CaO – 2.36%, Na2O – 4.21, K2O – 2.9%, Na2O/K2O = 1.45. Plagio-granites and plagio-migmatites inherit from the substratum rocks all minerals characteristic for amphibolite facies metamorphism. It should be notes that in the course of Berdychivski plagio-granites and plagio-migmatites development potassium input was more considerable although in the junction zone of Volynskiy and Dnistersko-Buzkiy mega-blocks Sheremetivski plagio-granites and plagio-migmatites get texture-structure properties similar to those of plagio-granites and plagio-migmatites of Berdychivskiy complex but relationships between the rocks of Berdychivskiy and Sheremetivskiy complexes are not established since their contacts are not studied in the given map sheet. Transitions between Sheremetivski and Zhytomyrski granitoids are established in drill-holes 4 and 7. The contacts are gradual, transition to Zhytomyrski granites is marked by increased amount of microcline, complete biotitization of amphibole, and muscovite appearing. In fact, Zhytomyrski granites are thought to be the products of the next granitization phase under high potassium activity. Petrophysical properties of Sheremetivski plagio-granites and plagio-migmatites: density – from 2.62 to 3 3 -6 -6 2.73 g/cm (σavg. = 2.69 g/cm ), magnetic susceptibility – 48×4π×10 CI units for granites and 92×4π×10 CI units for migmatites. Absolute age determined by K-Ar method on amphibole is 2430-2500 Ma [10].

Berdychivskiy complex (PR1bd)

The rocks of Berdychivskiy complex are widely developed in the map sheet area and occupy about 70% of the territory. This complex also includes autochthonous ultra-metamorphic rocks which are genetically and spatially linked with various Archean supracrustal, ultra-metamorphic and intrusive rocks comprising the

83 products of their granitization. At the modern erosion surface most widespread is their association with Bereznynska sequence gneisses of Dnistersko-Buzka Series. Berdychivskiy complex includes garnet-biotite with hypersthene migmatites (vinnytsites), biotite, garnet-biotite granites and migmatites, often with cordierite (Chudnovo-Berdychivski), garnet-biotite plagio-granites and plagio-migmatites, in places with cordierite, leucocratic granites, aplite-pegmatoid and pegmatoid granites. Mineral assemblages in the given rocks indicate their formation at the boundary between granulite and amphibolite metamorphic facies. These are highest-temperature, in comparison to the even-age (Zhytomyrskiy, Umanskiy, Kirovogradskiy complexes) granitoid rocks of Ukrainian Shield, which is expressed in orthoclase predomination over microcline, almost permanent occurrence of garnet and cordierite, somewhere hypersthene, and distinct bluish quartz coloring characteristic for the high-temperature varieties. Garnet-biotite migmatites and granites with hypersthene (vinnytsites) (mvnPR1bd). These rocks comprise transitional species between charnockitoids and garnet-biotite migmatites. Transitions of vinnytsites into charnockitoids and Chudnovo-Berdychivski granitoids are mainly gradual, unclear, reflecting increase in granitization degree. The rocks are studied in a number of outcrops and drill-holes. Vinnytsites display quite irregular grain size and opaque minerals distribution. Vinnytsites, observed in Chudnovo-Berduchivski granites, are leucocratic in composition with low, up to 1-2%, pyroxene content, while garnet content almost does not differ from that in granitoids. In melanocratic varieties, which are mainly observed at the contacts with charnockitoids, the finer-grained textures are developed. Garnet and biotite over there are commonly observed in more fine-grained places and pyroxene is often confined to pegmatoid enclaves. Garnet and pyroxene contents are in the reverse relations. Significant variations in mineral composition, reflecting substratum features and granitization degree, are expressed in petrochemical properties of vinnytsites: SiO2 content varies from 60 to 70%, Na2O – from 1.52 to 4.4%, K2O – from 1.87 to 4.61%. Macroscopically vinnytsites are grey, light-grey, greenish-grey, from fine- to coarse-grained, irregularly-grained, banded or massive rocks. Quite frequently the gradual transitions from hypersthene-garnet- biotite migmatites to leucocratic pyroxene-bearing garnet-biotite granites are observed, and then to biotite granites with single garnet grains or without garnet at all. Under microscope texture of vinnytsites is blasto-granitic, hetero-granoblastic with elements of porphyry-blastic and anti-perthitic. Structure is banded, parallel, massive. Mineral composition: plagioclase (oligoclase, rarely oligoclase-andesine) – 35-60%, orthoclase-perthite – 5-30%, quartz – from 10 to 30%, biotite – 3-10%, hypersthene – 1-15%, garnet – from single grains to 10- 15%, on places cordierite up to 3%. Accessories: zircon, apatite. Ore minerals include sulphides, rarely magnetite. Vinnytsites (pyroxene-garnet-biotite migmatites), despite of wide enough range of density – from 2.61 to 2.87 g/cm3 (for 95% of samples), exhibit single-modal histogram of density distribution (modal value – 2.75 g/cm3, average density – 2.76 g/cm3). Thus, average density of vinnytsites is higher than in Litynski enderbites 3 3 (σavg. = 2.73 g/cm ), and lesser than in enderbite-migmatites (σavg. = 2.82 g/cm ). These are mainly non-magnetic -6 -3 or low-magnetic rocks (æavg. = 76×4π×10 CI units, Iravg. = 61×10 A/m). In summary, vinnytsites are medium- density low-magnetic rocks. Above the fields of rocks under consideration the positive local gravity anomalies δga are observed, elliptic or slightly elongated, 0.3-0.6 mGal in amplitude, which coincide with the gentle negative magnetic field or, rarely, relative maximums in negative field 100-150 nTl in amplitude. In some cases the gradient zones of magnetic and gravity fields correspond to vinnytsites. Petrochemical parameters are given in Table 3.8. bt bt Biotite (γ ,γm mPR1bd), garnet-biotite, often with cordierite (γPR1bd) Chudnovo-Berdychivski granites and migmatites. These rocks comprise the major petrotype of the given complex, occupying about 50-60% of the territory and lacking only in the central part of Litynskiy dome. The rocks are studied in numerous outcrops and most of drill-holes. The contacts of these granitoids with actually all older rocks are established. The contacts are commonly not clear, gradual, reflecting increasing in granitization degree. Quite rarely the xenoliths are known with sharp contacts. The contacts with Archean pyroxene-bearing rocks (pyroxene mafic gneisses and gneisses, enderbites and charnockites) are often composed of vinnytsites (from the sites some centimeters thick to large enough zones and fields). At the contact with leuco-enderbites of Litynskiy complex the plagio-granites and plagio-migmatites are often developed (see below). The differences in the substratum rocks cause extreme discontinuity in structure and texture of Chudnovo-Berdychivski granites and essential variability in their mineral composition. The boundaries between migmatites and granites are being defined conventionally enough by occurrence of gneissosity and banding, in the lesser extent – by the ratios of major rock-forming minerals. Transitions between leuco- and melanocratic rock varieties also are gradual.

84 eters of Berdychivskiy complex rocks rocks complex of Berdychivskiy eters oefficients. Table 3.8. Average chemical composition and petrochemical param petrochemical and composition chemical Average 3.8. Table Note: see Table 3.1 and 3.2 for the meanings of petrochemical c petrochemical of meanings the for 3.2 and 3.1 Table see Note:

In the spot enclaves pegmatoid granites are often observed. Rarely these rocks are developed in the vein bodies of pegmatoid and aplite-pegmatoid composition which have clear cutting contacts. In the exo-contacts of alkaline rocks of Proskurivskiy massif phenitization zones are developed after Chudnovo-Berdychivski granites. Occurrences of garnet, biotite and cordierite in various proportions, as well as orthoclase (orthoclase- perthite) as the major potassium feldspar, were used as the major features for the definition of these group of rocks under the own name. Macroscopically Chudnovo-Berdychivski granites and migmatites are light-grey, grey, with greenish or pink shade rocks of various grain sizes, mainly medium-coarse-grained, with minor enclaves of fine-medium- grained varieties. Big enough (0.5-1 cm) grains of pink garnet are characteristic, which somewhere constitutes the bunches up to 2-3 cm in size, as well as scarce plagioclase porphyry-blasts up to 2-2.5 cm in size. Under microscope rock texture is granitic, blasto-ganitic, in places granoblastic, with elements of anti- perthitic and myrmekite. Mineral composition is variable in term of the rock-forming minerals but almost steady by their assemblage: plagioclase (oligoclase, oligoclase-albite, almost always with anti-perthite ingrowths) – from 20 to 40-45%, K-feldspar-perthite – 15-40%, quartz – 15-40% (commonly 20-30%), garnet – from single grains to 3- 5%, in places up to 15-20%, biotite – from 3-5 to 10-12%, cordierite – up to 5-7%, often sillimanite is observed, somewhere graphite. Accessories: apatite, zircon, monazite; ore minerals – sulphides, magnetite, ilmenite; secondary minerals – muscovite, sericite, chlorite, in places carbonate. Garnet-biotite granites and migmatites provide the background of the gravity and magnetic fields. These rocks are persistent enough by magnetic properties: magnetic susceptibility varies in the range 0÷70×4π×10-6 CI -6 units (æavg. = 39.5×4π×10 CI units). The range of density variations is somewhat wider: for granites average value is 2.68 g/cm3 with variations from 2.58 to 2.8 g/cm3; for migmatites – 2.76 g/cm3 with variations from 2.64 to 2.79 g/cm3 for 80% of samples. Average density value for granites and migmatites by two data sets is 2.79 g/cm3. Garnet-biotite granites and migmatites are expressed in the most widespread in the area type of physical fields – gentle or slightly differentiated negative magnetic field, background density values (areas of prevailing granites and migmatites), or the negative field of local gravity anomalies from -0.25 to -1.0 mGal (areas of prevailing granites). Garnet-biotite, in places with cordierite plagio-granites (pγPR1bd) and plagio-migmatites (pγmPR1bd). These rocks are actually identical to Chudnovo-Berdychivski granites and migmatites by the opaque rock- forming mineral assemblages and contents, and visually do only differ in somewhat darker shades of light-grey coloring and lack of pink shades. The rocks are widely developed in the external zone of Litynskiy dome where they often constitute the envelopes around the leuco-enderbite bodies of Litynskiy complex. Apparently these rocks most often had comprised substratum of plagio-granitoids. It should be noted that plagio-granites exhibit the lowest average silica content (61.8-66.36%) among the granitoids in the area, which is lower than average silica content in leuco-enderbites. One can assume that granitization process with sodium input had accompanied by slight silica removal. Plagio-migmatites and plagio-granites constitute the core portions of antiforms (compression zones) within two-feldspar potassium granitoids which fill up the synforms (extension zones). The rocks are mainly developed to the south-west from Khmilnytska fault zone. The rocks often contain xenoliths of Dnistersko-Buzka Series rocks, mainly mafic gneisses of Tyvrivska sequence. In the center of the area the rocks surround the fields of garnet-biotite gneisses of Bereznynska sequence and constitute the sites of plagio-granitization therein. There are no considerable differences by structure-texture features between plagio-granites and plagio-migmatites; the differences are only noted in more or less expressed gneissosity and banding. Macroscopically these are grey, light-grey, massive or banded rocks. Under microscope texture is granoblastic, hetero-granoblastic, rarely porphyry-blastic. The rock composition changes from plagio-granite to tonalite. Average mineral composition: plagioclase (oligoclase, albite-oligoclase-anti-perthite) – 30-45%, K- feldspar (commonly orthoclase-perthite) – from 3-7 to 15%, quartz – 20-30%, garnet – 5-15%, biotite – 3-7%, in places cordierite – from single grains to 3-5%; sillimanite and graphite are noted. Accessories: apatite, zircon, monazite. Ore minerals: ilmenite, magnetite, sulphides. At the low enough for granites silica content, plagio-granites and plagio-migmatites exhibit high and steady enough content of Na2O – 4.18-5.06% at K2O content 1.34-2.82%. The ratio Na2O/K2O is 2-3. Magnetic properties of plagio-granites and plagio-migmatites are steady enough: for 95% of measures -6 -6 samples magnetic susceptibility does not exceed 70×4π×10 CI units, æavg. = 48×4π×10 CI units. Density 3 3 variations are wider: in 70% of samples density is 2.58-2.70 g/cm , in 18% of samples – 2.70-2.82 g/cm , σavg. = 2.69 g/cm3. Magnetic varieties are encountered in drill-holes where pyrrhotite is developed in the rocks. Physical

86 properties of these rocks are similar to those of garnet-biotite granites. In the physical fields these rocks are expressed in the negative local gravity anomalies 0.3-0.5 mGal and negative magnetic field. ap Leucocratic (lγPR1bd), aplite-pegmatoid, pagmatoid (γ PR1bd) granites. Leucocratic granites include pink-grey, light-grey diverse-grained rocks with very low content of opaque minerals, specifically, biotite, garnet, very rarely cordierite, and essential potassium feldspar (orthoclase-perthite) predomination over plagioclase. The rocks are observed within typical Chudnovo-Berdychivski granites, related to them with gradual transitions and are developed in the enclaves of irregular shape, rarely in the bands. Somewhere these enclaves (mainly but not completely consisting of the given rocks) are big enough in size (up to 8 km2). Transitions of leucocratic granites to the aplite-pegmatoid and pegmatoid varieties are also gradual, and two latter varieties, in turn, exhibit gradual transitions one into another. The large fields of leucocratic granites are confined to the tectonic breaks of north-western and sub- latitudinal strike or located in the cores of granite domes, that is, are related to the extension zones with extensive K-feldsparization. Big enough bodies of aplite-pegmatoid granites are located within the fields of leucocratic granites. Minor massifs with allochthonous patterns and the vein bodies of aplite-pegmatoid and pegmatoid granites with clear cutting contacts are known over entire studied area. By mineral composition all mentioned rock varieties are quite identical: potassium feldspar predominates (normally orthoclase-perthite, rarely microcline-perthite) – 40-75%, quartz – up to 40%, plagioclase (albite-oligoclase) – 10-15%, in places up to 30%, or lacking at all. Content of opaque minerals is 1- 5%, almost always biotite is observed, rarely garnet. Accessories: apatite, zircon, monazite. By chemical composition (see Table 3.8) the rocks are enriched in SiO2 – up to 76.2% and alkali Na2O+K2O up to 17.08%. Leucogranites exhibit steady low density values (2.63 g/cm3 in average with the range from 2.58 to 2.70 g/cm3 for 85% of measured samples). They comprise the lightest varieties of Berdychivskiy complex. The rocks are almost non-magnetic, average magnetic susceptibility is 34×4π×10-6 CI units, residual magnetization does not exceed 22×10-3 A/m. In the gravity field the rocks are expressed in the local gravity minimums from -0.7 to - 1.0 mGal in amplitude, which coincide with the gentle negative magnetic field. 3 Pegmatoid and aplite-pegmatoid granites also display steady low density (σavg. = 2.82 g/cm with the range from 2.55 to 2.69 g/cm3). About 70% of measured samples are almost non-magnetic or low-magnetic -6 -6 while magnetic susceptibility varies from 0 to 600×4π×10 CI units, æavg. = 99×4π×10 CI units, and in 30% of measured samples magnetic susceptibility is higher in the range 100-300×4π×10-6 CI units because of magnetite and pyrrhotite occurrence in the rocks. Pegmatoid and aplite-pegmatoid granites are expressed in the local oval or extended along faults gravity minimums up to -2.4 mGal, which coincide with negative magnetic field. Contents of lithophyle and chalcophyle elements (except molybdenum) in all granitoids of Berdychivskiy complex are low or decreased as it is evidenced by their concentration coefficients: Li – 0.2-0.8, Y, Yb – 0.3-0.5, Sn – 0.3-0.5, whereas contents of siderophyle elements are high enough: Ni – 3.4-17.5, Cr – 3.0-15.6, Co – 1.4-3.2 [18]. This probably indicates that Early Proterozoic high-temperature granitization in general is accompanied by removal of litho-chalcophyle trace elements and lack of favorable conditions for their accumulation. At the same time, inheriting substratum rocks geochemical specialization, they exhibit high enough (as for granitoids) contents of siderophyle group elements. Increased values of chalco-lithophyle group elements are noted at the sites with superimposed processes of metasomatism and hydrothermal re-working and all high-contrasted anomalies and points of increased mineralization of the rare-earth and radioactive elements, encountered in the rocks of Berdychivskiy complex, are related to these zones.

Zhytomyrskiy complex (PR1žt)

In the given territory Zhytomyrskiy complex includes biotite and two-mica two-feldspar granites (γPR1žt) intersected to the north-west from Teterivskiy fault by drill-holes 3, 4, 7, where these rocks alternate with plagio-granites and amphibole-bearing granitoids of Sheremetivskiy complex. The separate massif of Zhytomyrski granitoids is distinguished on results of geophysical data interpretation close to the northern map sheet border in between Mykulyn and Karpylivka villages. Macroscopically these are grey, in places pink-grey, fine-medium-grained, mainly regularly-grained granites with massive structure. Somewhere they display unclear banding caused by sub-parallel arrangement of biotite flakes. Under microscope the rock texture is hypidiomorphic, granitic, in places cataclastic. Mineral composition: plagioclase (albite-oligoclase) – 35-45%, K-feldspar (microcline) – 25-30%, quartz – 20-30%, biotite – 5-10%, in places muscovite up to 1%. Accessory minerals: apatite, monazite, magnetite, ilmenite, pyrite.

87 Plagioclase (albite-oligoclase) is developed in elongated and irregular tabular grains, in places with antiperthite microcline ingrowths. Grain size is 1.0-4.0 m. Microcline is observed in the irregular grains, rarely in anti-perthite ingrowths. Some grains contain fine plagioclase ingrowths. Microcline crystal size is up to 2.0 mm. Quartz is developed in the grains and allotriomorphic intergrowths which fill the space between other minerals, rarely in the inclusions in feldspars. Extinction is wavy. Biotite is observed in the elongated flakes which, like quartz, fill up the space between other minerals. The flakes commonly are diverse-oriented except the rock varieties with unclear-banded structure. Somewhere, besides biotite, fine muscovite flakes are also noted. Apatite in places is observed in the rounded big enough grains 2×2.5 mm in size. Zircon is confined to biotite flakes. The crystal size is up to 0.1 mm. Magnetite is observed in the scarce, relatively idiomorphic grains or their intergrowths, positioned between quartz and feldspars, often in association with biotite. Grain size is 0.1-0.2 mm. The chemical parameters (data set is insufficient, n=3) of Zhytomyrskiy type of granites in the studied area are as follows: SiO2 – from 67.75 to 70.62%, Al2O3 – 13.44-14.89%, Fe2O3 – 2.13-4.56, FeO – 1.36-1.89, TiO2 – 0.26-0.55, MnO – 0.03-0.05%, CaO – 0.44-2.43%, MgO – 1.68-2.07%, K2O – 1.82-3.33%, Na2O – 1.45- 3.75%, Na2O/K2O ~ 1.0. Granites of Zhytomyrskiy complex, according to A.S.Voynovskiy [17], exhibit positive geochemical specialization for Cr, Ni, and negative for Li, Y, Yb, Sn, Be, that is, by these parameters they almost do not differ from the rocks of Berdychivskiy complex. Unfortunately, in the statistic calculations just the leucocratic and aplite-pegmatoid granites were involved due to lack of spectral analyses for other rock varieties of Zhytomyrskiy complex in the given area. 3 -6 Zhytomyrski granites are low-density (σ. = 2.61 g/cm ) and magnetic (æavg. = 42×4π×10 CI units). -3 Residual magnetization Ir = 65×10 A/m. In the gravity and magnetic fields the massifs of these rocks are expressed by the local negative gravity anomalies 1.5-2.5 mGal in amplitude and negative magnetic anomalies of various intensities.

26Retrograded, hydrothermally-metasomatically and tectonically altered rocks, tectonites

Retrograde metamorphic processes are most prominent after pyroxene-bearing rocks of Dnistersko- Buzka Series and vary rarely after charnockitoids. They are expressed in the replacement of high-temperature mineral assemblages by the lower-temperature ones. Most altered are pyroxenes which are replaced by amphiboles, biotite, serpentine, bastite, and carbonates. In places several alteration stages are observed when amphibole is developed after pyroxene and, in turn, is replaced by biotite and the latter – by chlorite. Pyroxene modification products also include magnetite. Plagioclase is commonly replaced by the K-feldspar-chalcedony aggregate, with minor carbonate, oxide hydroxides, and kaoline. In places scapolitization is noted. Garnet in retrograded zones is resorbed, with inclusions of biotite, often magnetite, and iron hydromica. The biggest sites of retrograded rocks are noted in the zone of Khmelnytskiy fault. Metasomatic and hydrothermal rock modifications are related to the tectono-magmatic activization in Paleo-Proterozoic and, probably, later. They are tightly related to the faults set up and activated over these periods. Most extensively metasomatic processes are released in phenite formation related to alkaline and sub- alkaline rocks of Proskurivskiy complex. Most often in the studied area silicification processes are observed which are mainly developed along linear tectonic breaks. Silicification is expressed both in the extensive quartz penetration over entire rock mass and in the quartz veins and veinlets up to 0.3-0.5 m thick, as conformable as the cutting ones. Under extensive silicification the band-like units are formed composed of quartz by 50-75%, in places more. Some feldspar and opaque mineral (commonly biotite) grains are preserved in quartz. Silicification is often accompanied by sulphidization and graphite and molybdenum re-distribution into enriched units (Kutyshche, Maliy Brataliv and other villages). Microclinization and albitization are most extensively developed in Khmeltynska and Khmilnytska tectonic zones. The process is expressed in various modes in different rocks. In granitoids of Berdychivskiy complex, where K-feldspar is normally orthoclase (orthoclase-perthite), the process is clearly marked by the second generation of potassium feldspar – microcline-perthite, rarely lattice microcline. Development of this mineral makes the rock pink-colored and in general is not characteristic for the granitoid fields (except

88 Khmilnytski). In Khmilnytska zone development of replaced pegmatites with rare-earth mineralization is related to superimposed microclinization. In Khmelnytska zone extensive microclinization is observed in places where the rocks of Proskurivskiy complex are developed (Goloskiv, Rudnya, Antonivka, Verbka villages). The rock albitization is also observed in the same places but in much lesser extents. Most extensively albitization is developed in Khmilnytska fault zone. It is expressed in plagioclase sodification with albite rims and somewhere (Zhdanivka village) albite is developed in separate veins and veinlets which control uranium mineralization. Epidotization and chloritization, in places carbonatization, are confined to Khmelnytska and Teterivska fault zones. Commonly this alteration is developed after the rocks of Proskurivskiy and Sheremetivskiy complexes noted at Goloskivska and Brazhynetska sites. Cataclasites, blasto-cataclasites, milonites and blasto-milonites are noted in numerous drill-holes. These rocks constitute the zones from some to hundreds meters and in Khmilnytska fault zone up to 1 km and more in size. In cataclasites and blasto-cataclasites cataclastic and blasto-cataclastic, in places blasto-cement textures are observed. Structure of these rocks is normally schistose, and after granitoids grey augen gneiss-like rocks are developed. Cataclasites after gneisses and mafic gneisses differ in the melanocratic composition only. At the sites of extensive cataclasm of leucocratic and aplitoid granitoids the rocks get granulite-like appearance. In milonitization zones the primary rocks are grinded, sheared with formation of coarse-micro- milonitic, blasto-milonitic textures, in places breccia-like. Commonly they are dark-grey to black. Milonites after leucocratic granitoids are light- or pink-grey. Silicification, microclinization, biotitization, chloritization and other processes are commonly developed after tectonites. Thickness of milonites varies from some centimeters to 18 m (DH 18244) [47]. In case of extensive dynamo-metamorphic processes blasto-cataclasites and blasto-milonites essentially affect the physical fields. The best example is Khmilnytska fault zone which is clearly expressed in the gravity field with negative δga anomalies. Garnet-biotite granites and plagio-migmatites, constituting most part of the zone, are by 0.03-0.05 g/cm3 less dense than non-deformed granites and plagio-migmatites. According to data of V.D.Geyko [22] based on the great number (some hundreds) of average density measurements for the common rock types developed in Khmilnytska zone and Litynskiy block, the rock density (enderbites, garnet-biotite granites, vinnytsites) differs by 0.11 g/cm3, 0.08 g/cm3 and 0.05 g/cm3 respectively. Average values of magnetic susceptibility and residual magnetization for the rocks like enderbites, charnockites and vinnytsites in Khmilnytska fault zone drop down by 1.5-5 times.

54. WEATHERING CRUST

Weathering crust of crystalline rocks is developed almost everywhere in the eastern and central part of the studied map sheet, except the ancient and modern erosion sites in the river and gully valleys, and relatively elevated basement blocks; the crust is absent in the west, on the slope of Ukrainian Shield. The crust is developed in the blanket of variable thickness and is overlain by Paleogene, Neogene and Quaternary sediments (Fig. 4.1). Composition, distribution and thickness of weathering crust are caused by the basement rocks composition, their structure-texture features, fracturing and crushing degree, paleo-geographic conditions over the time of crust development, erosion intensity, cutting degree of the ancient and modern relief. Most favorable conditions for weathering crust development existed in Mesozoic and Cenozoic. By genetic and morphological features the planar and linear weathering crusts are distinguished. The planar weathering crust predominates in the studied area and its thickness is 10 m in average. Linear weathering crust is confined to the zones of tectonic breaks and is only distinguished by increased thickness. Maximum thickness of linear weathering crust attains 168.3 m. By the composition of mineral assemblages and relations between the newly-formed and relict minerals the following zones are distinguished in the column of weathering crust (from bottom to top): 1. Zone of disintegration and initial dismembering where primary rock minerals predominate with their initial dissolution and hydration – e1Mz-Kz. 2. Zone of intermediate dismembering (hydromica, kaolinite-hydromica, montmorillonite-hydromica) with prevailing hydromica, kaolinite and montmorillonite development, and a number of altered feldspar and opaque minerals – e2Mz-Kz. 3. Zone of final leaching with predominate kaolinite and montmorillonite – e3Mz-Kz. In weathering crust developed after quartz-bearing rocks the quartz relicts are observed in all zones. In general, the rocks constituting specific zones, do not have clear boundaries and are gradually substituted one by another making definition of the zones conventional a bit. In the map sheet area the planar kaolinite-hydromica and hydromica-kaolinite weathering crust is mainly developed, except Teterivska tectonic zone, where the zone of disintegration and initial dismembering predominate. Weathering crust is being formed after all varieties of crystalline rocks. Depending on their composition, weathering crust profiles differ in structure and thickness (both individual zones and total). Weathering crusts comprise important source of minerals. Occurrences of primary kaoline, graphite, apatite, vermiculite, rare-earth metals, titanium, as well as mineralization points of titanium, zirconium, tungsten, monazite, garnet, copper, tin, molybdenum, nickel, and gallium are related to these rocks.

27Weathering crust of granitoid rocks

The crust of this kind occupies up to 80% of the total square of weathering crust. Structure of the crust is similar and three zones are distinguished (from bottom to top): - zone of disintegration and initial dismembering - hydromica-kaolinite zone - kaolinite zone. Maximum thickness of weathering crust after granitoids attains 96.0 m. Disintegration and hydromica- kaolinite zones are most developed. Kaolinite zone after granitoids is less developed but is thicker. Zone of disintegration and initial dismembering (e1). Transition of this zone into primary rocks is gradual, and to the higher zones – sharp enough. Average thickness of the zone is 4-5 m, in places up to 50 m. The rocks in this zone are fractured, weathered, often modified to gruss, slightly kaolinitized. Feldspar becomes dirty, kaolinitzed, and opaque minerals are chloritized. Major structure-texture features and color of primary rock are preserved and the color is lighter, mainly with grey shade. Hydromica-kaolinite zone of weathering crust (e2) is widespread. Average thickness of the zone is 6-8 m, in places up to 70 m. Maximum thickness is observed at the sites of linear weathering crust. The rocks in this zone are spot-colored, greenish-grey, the primary rock texture is preserved. Feldspars are completely replaced by kaolinite, biotite – by hydromicas, and pyroxenes (in enderbites, charnockites) – by montmorillonite. Amount of newly-formed minerals in weathering crust attains 90%, of these kaolinite – 45-80%, hydromicas – 10-45%. In this zone the upward gradual increasing of weathering processes is observed – lightening of secondary minerals in weathering crust.

Grytsiv

Lyubar

Starokostyantyniv

Stara Synyava

KHMILNYK

Medzhybizh Khmelnytskiy

South Boug Letychiv

South Boug

5 kilometers in 1 centimeter

Fig. 4.1. Geological map of weathering crust in the map sheet M-35-XXII (Starokostyantyniv).

Zones of weathering crust: 1 – kaolinite, kaolinite-nontronite; 2 – hydromica-kaolinte, kaolinite- hydromica, kaolinite-montmorillonite-hydromica; 3 – disintegration zone; 4 – unchanged rocks; 5 – planar weathering crust boundaries; 6 – boundaries of sediments overlaying weathering crust: a) Neogene, b) Paleogene, c) Vendian; 7 – a) isohypses of weathering crust and crystalline basement, b) isopachs; 8 – linear weathering crust; 9 – drill-holes, intersected full profiles of weathering crust and their numbers.

Kaolinite zone (e3). This zone of weathering crust is mainly developed in the eastern part of the area. Thickness of this zone is 7.5-9.0 m in average, and in some places it attains 90 m. The rocks of the zone comprise light-grey, almost white primary kaolines with scarce brown spots of iron hydroxides and quartz grains. Content of the latter is from 15 to 45% and quartz amount gradually increases upward in the column. In the lower part of this zone minor hydromicas are observed, especially in cases of charnockites.

28Weathering crust of biotite, garnet-biotite, cordierite-garnet-biotite, graphite-biotite gneisses

In the studied area this kind of weathering crust is locally developed. In the profile of this type three zones are distinguished. Zone of disintegration (e1) is developed almost everywhere and includes kaolinitized, highly weathered and fractured gneisses. Average thickness is 5 m. In some drill-holes thickness is up to 30 m. Texture of primary rock is preserved and visual difference of the zone rocks from primary ones is in prominent lightening. Upward in the zone the rocks become lighter because of increased kaolinitization of feldspars. Biotite is hydrated and substituted by hydromica. Quartz remains unchanged. Kaolinite-hydromica zone (e2) is widely developed with average thickness 12.5 m. In some drill-holes thickness of the zone is up to 40 m [32]. The rocks are green-grey and consist of kaolinite – 25-40%, quartz – 10-30%, hydromica – 40-65%, and microcline – up to 10%. Kaolinite zone (e3) is less developed than two first ones. Its average thickness is 9.0 m, in some cases high enough [28]. Kaolinite zone is composed of white, light-grey rocks, mainly greasy in touch. Mineral composition: kaolinite – 70-80%, quartz – 15-25%. Quartz is notably corroded and extensively cut by the fine fracture network.

29Weathering crust of pyroxene, garnet-pyroxene, amphibole, biotite-amphibole gneisses and mafic gneisses

Three zones are distinguished in this type of weathering crust: - disintegration and initial dismembering; - kaolinite-montmorillonite-hydromica; - kaolinite. Thickness of this weathering crust is 9 m in average and in some drill-holes – up to 85.0 m. These weathering crusts are similar to those of biotite gneisses and differ in low quartz content, montmorillonite development and more extensive green color. The third zone visually differs from the same zone in weathering crust of biotite gneisses in the greenish shade. Average thickness of kaolinite zone is 8 m. In some drill-holes thickness of kaolinite zone is up to 39 m [44].

30Weathering crust of gabbro, gabbro-amphibolites, diabases, gabbro-diabases, monzonites and gabbro-monzonites, pyroxenites

In the studied area this crust is locally developed. Average thickness of weathering crust is 5 m. It includes three zones but these are not intersected in all drill-holes. Brazhynetskiy vermiculite occurrence is related to weathering crust of this type. Disintegration zone (e1) is developed in the area more extensively than two other ones and thickness of the zone is up to 5 m, in places more. The zone consists of grey, yellowish-greenish-grey rocks, lighter, than primary ones because of biotite, amphibole and pyroxene substitution by hydromica and chlorite, and leucocratic part – by kaolinite. Kaolinite-montmorillonite-hydromica (e2) zone of weathering crust in general exhibits spotty coloring, the rocks are grey-green, yellowish-grey, with well-preserved texture and structure of primary rocks. Accumulations of bluish-green hydrochlorite and brownish-yellow hydromica are observed. The rocks in the zone comprise the mixture of montmorillonite, hydromica and minor kaolinite. Relic minerals include quartz, K- feldspar, apatite, ore minerals. Average thickness of the zone is 5 m. Kaolinite-nontronite, kaolinite-chlorite-nontronite (e3) zone of weathering crust is greenish-grey to green-brown, with yellowish-brown spots, quartz-less. It is distinguished in some drill-holes, average thickness is 9 m. The rocks in the zone are composed of kaolinite, nontronite, chlorite with minor hydromica. After

92 spectral analysis of samples from the zone (DH 49, Zhdanivskiy massif), content of platinoids is 0.02-0.04 g/t, nickel – 0.1-0.2%, cobalt – 0.01-0.02%.

31Weathering crust of syenites

In the studied area it is very rarely observed, average thickness is 12 m. Weathering crust of this type includes three zones. Texture of primary rocks is well-preserved over entire crust profile. Zone of disintegration and initial dismembering (e1) of primary rocks consists of kaolinitized and weathered syenites. Thickness of the zone is low but in some drill-holes it attains 6.5 m [51]. Transition into fresh unaltered rocks is gradual. Visual differences of the rock from the fresh one include lightening and fracturing. Mineral composition: feldspars – 85-90%, biotite – 5-10%, quartz – 1-5%, pyroxene – up to 1%. Hydromica-kaolinite zone (e2) is composed of light-grey to white, often with greenish shade rocks. It is composed of completely kaolinitized feldspar, hydromica and minor quartz. Thickness of the zone is 9 m, in some drill-holes – up to 30 m. Kaolinite zone (e3) is composed of white, light-grey rocks, greasy in touch. Average thickness of the zone is 25 m. Mineral composition: kaolinite – 90-95%, quartz – 1-5%. Feldspar is completely kaolinitized, often pelikanitized. By mineralogical analysis, ilmenite, apatite, zircon, and monazite are identified, as well as molybdenite signs.

65. TECTONICS

The studied map sheet is located in the western part of Ukrainian Shield, at the junction of two mega- blocks – Volynskiy and Dnistersko-Buzkiy. The far western part of map sheet belongs to the western Shield slope with the eastern boundary set by the Vendian sediments margin. Geological column in the area includes high-deformed and metamorphosed Archean-Proterozoic units of crystalline basement (lower tectonic level) and Vendian-Phanerozoic sedimentary units of the platform cover (upper tectonic level).

32Lower tectonic level

The lower tectonic level consists of litho-tectonic complexes (LTC) developed in different geodynamic conditions. In Podilska LTZ formations of initial lithosphere consolidation, collision environments and internal plate areas are developed. Initial lithosphere consolidation environments are expressed in the LTCs of enderbite-granulite paleo- zone: sequentially developed granulite-basite and kinzigite formations (NG1-AR1) and products of their plagio- granitization under conditions of granulite facies – enderbite-migmatite (NG2-AR1). Granulite-basite formation is mainly composed of meta-basaltoids of Tyvrivska sequence and ultrabasites (meta-basites) of Sabarivskiy intrusive complex. Kinzigite formation includes meta-sedimentary and meta-volcanic rocks of Bereznynska sequence. Enderbite-migmatite formation is composed of gneiss-like enderbites of Gayvoronskiy complex. The LTCs of collision environments in the deep compression paleo-zone have been developed in three stages: early, late collision, and final phases of late collision. The charnockite formation (KG1-AR2), composed of leuco-enderbites and charnockites of Litynskiy complex, corresponds to the early collision. The late-collision kinzigite-granite formation (KG2-PR1), composed of diverse granitoids of Berdychivskiy complex, is most developed in the studied area. The leucogranite formation (KG3-PR1), composed of allochthonous granites of Khmilnytskiy complex, does correspond to the final phases of late collision. The internal plate environments include formations of hot-spot and lines paleo-zone developed at various phases in different tectonic structures: alkali-gabbroid (GT1-PR1) and dyke (GT2-PR1). In the alkali-gabbroid formation, developed in sub-latitudinal Khmelnytska tectonic zone, the rock range of Proskurivskiy complex varies from ultramafic, mafic alkaline and sub-alkaline, to felsic alkaline and sub-alkaline. The dyke formation, confined to Khmilnytska tectonic zone and related breaks, include diabase and gabbro-diabase dykes. Tectonic patterns in the different parts of the territory are mainly defined by one or another LTCs. In the basement of Volynska LTZ the distinct Paleo-Proterozoic metamorphosed sedimentary- volcanogenic rocks are developed (Vasylivska Suite) related to the setting up the continental paleo-rift over Archean proto-crust at the boundary between Archean and Proterozoic (KR1-PR1). Upon the short-term collision phase at about 2400 Ma, accompanied by plagio-granitoids of Sheremetivskiy complex (KG1-PR1), the rift was expanded and transformed in large enough basin, where, outside the studied area, the rocks of upper part of Teterivska Series were depositing. Transitional zone sea-continent, which apparently encompassed the northern part of studied map sheet, was developing under conditions of active continental margin in the litho-tectonic paleo-zone of igneous arch, as it is indicated by gabbro-monzonite formation (Bukynskiy complex) (AM2-PR1). With the collision phase at about 2000 Ma granite-migmatite formation (Zhytomyrskiy complex) (KG2- PR1) is related over there. Tectonic patterns of the area match well the gravity and magnetic fields. As noted above, the territory is positioned in two mega-blocks – Dnistersko-Buzkiy and Volynskiy, which in the area are comprised of two I- order blocks: Podilskiy and Novograd-Volynskiy. Position and structure of the boundary between Dnistersko-Buzkiy and Volynskiy mega-blocks are disputable. In the published and prepared to publishing map sheets of Derzhgeolkarta-200 “Fastiv” and “Skvyra” this boundary is set by Andrushivska fault zone. In the map sheet “Zhytomyr” it follows Krasnogorsko-

94 Zhytomyrska and Teterivska fault zones. Analysis of physical fields and litho-tectonic complexes in Podilskiy and Volynskiy mega-blocks in the given map sheet and adjacent ones allow assumption that Teterivska zone in the inter-block one in the studied area. Some role is also played by the faults of Andrushivska zone, which shift out Teterivska zone in the sub-latitudinal direction, making the mega-block boundary patterns intricate and broken. The I-order Podilskiy block, in turn, by the system of intra-block fault zones is divided into the II-order blocks: Vinnytskiy, Berdychivskiy, Khmelnytskiy; Novograd-Volynskiy block in the studied area is represented in the area by the II-order Shepetivskiy block. The second-order blocks are further divided into the higher-order blocks which differ in structure and composition. The south-western part of the area belongs to the eastern part of the II-order Khmelnytskiy block, which coincides in space with the same-named regional gravity maximum up to 40 mGal in the center. In the block formations NG1+NG2-AR1 and KG1-AR2 are mainly developed which underwent partial re-working in Paleo- Proterozoic. The south-eastern part of the area belongs to the north-western part of Vinnytskiy block, where III-order Litynskiy block is distinguished, which coincides in the space with Litynskiy gravity maximum. In the magnetic field the arc-shaped, linear or irregular positive magnetic anomalies 2000-4000 nTl in amplitude are distinguished in this area. In this structure the rocks of migmatite-enderbite (NG2-AR1) and charnockite (KG1- AR2) formations are developed composed of enderbites and charnockites of Litynskiy complex, occurring within the rocks of kinzigite-granite formation (KG2-PR1). The north-eastern part of the area belongs to the II-order Berdychivskiy block, specifically, its western part, including III-order Ivanopilskiy and Ulanivskiy blocks. In the map sheet area Ivanopilskiy block in the gravity field is expressed in the well-differentiated alternating local ga anomalies -1.8…+2.0 mGal. In the block the rocks of both kingizite and granulite-basite formations (NG1-AR1) are developed, preserved within the rocks of charnockite (KG1-AR2) and kinzigite-granite (KG2-PR1) formations. The far north-western part of the area belongs to the marginal part of Volynskiy mega-block, in fact, to the inter-block zone 12 km wide (Teterivskiy fault), providing respective gravity field with low-intensity (up to

12 mGal) gravity anomalies ga extended in the north-eastern direction. Over there, the rocks of terrigenous- volcanogenic (KP-PR1), plagiogranite-migmatite (KG1-PR1), and granite-migmatite (KG2-PR1) formations are developed. The central part of the area is mainly composed of the kinzigite-granite formation rocks. Structure is complicated by the granite domes (Starosynyavskiy, Paplynetskiy and Sluchanskiy), numerous faults and related secondary alteration of the rocks.

65Tectonic blocks

II-order Khmelnytskiy block

In the map sheet area the north-eastern part of this block is situated, occupying almost 80% of the territory; from the east it is bounded by Yablunivsko-Bilokorovytska deep-seated fault zone, from the north-east – by Khmilnytska zone (its north-eastern branch), from the north-west – by Teterivska zone, and from the north- by Andrushivskiy fault. In the gravity field Khmelnytskiy block comprises the area of the highest positive gravity field, from 22-24 mGal at periphery to 40 mGal in the central part. In the zone of local gravity anomalies (L = 6 km) the block in general is expressed in the well-differentiated alternating anomalies ga from -2.0 to +3.8 mGal, isometric (1-4 km in diameter) or linear, with various orientation of their long axes. Magnetic field, as noted above, is quite complicated, varying from -950 to +1000 nTl. In general, the II-order Khmelnytskiy block by the physical fields, geological structure and formations is divided into the III-order Medzhybizkiy, Veselivskiy and Starosynyavskiy blocks.

Medzhybizkiy block

The major tectonic element in this block is the same-named dome structure, where at the basement surface Paleo-Archean rocks are exposed – mafic gneisses and gneisses of Tyvrivska sequence, meta-basites of Sabarivskiy complex and enderbites of Gayvoronskiy complex. The latter are essentially reomorphosed. In the gravity field this dome structure corresponds to Khmelnytskiy gravity maximum up to 40 mGal. In magnetic field this is contrasted area of positive values Ta (Za) in the range 100-4000 nTl, consisting of band-like and linear (up to 9 km long) arc-shaped, from the north-west to sub-latitudinal extension, which are arranged in the

95 semi-closed ring structure and impose an effect of zoned patterns in the anomalous magnetic field. Further to the east some minor north-east and north-west magnetic anomalies from 200 m to 3 km in size are observed (for instance, “Rudnya” anomaly), arranged in the semi-closed ring structure and creating effect of zoned patterns in anomalous magnetic field. Mentioned zonation is caused by multiple influences of superimposed processes that changed the rock appearance and their properties during activization periods. High-temperature retrograde metamorphism at the stage of enderbite formation and subsequent charnockitization resulted in the rock decomposition and iron separation in magnetite; this is why in most cases high-intensity positive magnetic anomalies are accompanied by the gravity minimums. Positive magnetic anomalies in combination with positive local gravity anomalies do correspond to the sites composed of mafic gneisses and gneisses of Tyvrivska sequence, and meta-basites of Sabarivskiy complex. Mosaic patterns of magnetic field are caused by the development of Litynskiy complex charnockitoids in this part of Medzhybizkiy block, which comprise the least dense rocks, expressed in the local gravity minimums that are thought to be superimposed antiforms. The sites of most extensive positive residual gravity anomalies (2 mGal and more) on the background of alternating magnetic field do correspond to the intrusive massifs of Proskurivskiy complex sub-alkaline gabbroids. The southern part of Medzhybizkiy block is most elevated, as it is evidenced by the combined positive gravity field with positive magnetic anomalies, typical for the deep erosion cut of the basement, and results of density modeling [51]. The northern block part is subsided by sub-latitudinal fault (along line Khmelnytskiy- Medzhybizh) of Khmelnytska tectonic zone, and at the basement erosion cut level it is mainly composed of granitoids of Berdychivskiy complex, as it is expressed in the physical fields (negative magnetic, positive gravity). According to the rock density and magnetic modeling, the rocks dipping in the II-order Khmelnytskiy block is sub-vertical in general [51]. Medzhybizkiy block from the north-east is separated from Starosynyavskiy block by Letychivska fault zone of the north-western extension, and from the north from Veselivskiy block – by the far northern fault of Khmelnytska sub-latitudinal zone.

Veselivskiy block

It is located to the north from Medzhybizkiy block. In the north-east by Letychivska tectonic zone is adjoins Starosynyavskiy block, and Teterivska fault zone comprises its northern boundary. Magnetic field of the block contains the north-east-trending zone of high-contrasted, patterned positive anomalies Ta. The internal local anomalies Ta, providing mosaic structure, vary in strike from sub-latitudinal to north-western; these anomalies are linear, arc-shaped, arranged in the ring structures and individual isometric positive anomalies from 0.3-0.4 km to 2-3 km across (Veselivka, Mykhaylivtsi, Pidgirne villages). The gravity field of the block contains two positive elliptic anomalies ga, separated by tectonic zone (2- 3 km wide) of the north-eastern extension (by line Lagodyntsi village – Starokostyantyniv town), orthogonal to Letychivska tectonic zone. The first positive anomaly ga is located in the area of Zaruddya – Redvyntsi – Mytkivtsi villages. Its intensity at maximum is 33 mGal and strike of north-western. The second positive anomaly ga is less intensive (25 mGal at maximum), it is located to the north-west, north-east-trending, and extended outside the studied area. Both anomalous zones of ga field (their major parts) coincide with the negative magnetic field, and the high-contrasted area of positive Ta field is located in between. The gravity and magnetic fields of Veselivskiy block suggest for the wide development (at the level of erosion cut) of garnet-biotite granites of Berdychivskiy complex, charnockitoids of Litynskiy complex, and in lesser extents the rocks of Dnistersko-Buzka Series (gneisses and mafic gneisses).

Starosynyavskiy block

This one is located in the central part of the studied area. In the south-west it is bounded by Letychivska fault zone, and in the north-east and east – Khmilnytska and Bilokorovytska tectonic zones respectively. Magnetic field of the block is mainly gentle, negative, from 0 to 950 nTl in values. On this background single minor (from 0.2 km to 5 km in size) elliptic or linear local magnetic anomalies 100-4000 nTl in amplitude and various strikes – from longitudinal to latitudinal – are observed. In the gravity field two ga maximums 26 and 27 mGal and a range of minor ones (Zalissya, Podolyany and other villages) are noted. Within local gravity anomalies some major isometric maximums and a range of

96 minor minimums of various shape and amplitude are distinguished, which are confined to Letychivska and Khmilnytska tectonic zones. These patterns of physical fields are caused by the wide development of Paleo-Proterozoic garnet- biotite granites and migmatites of Berdychivskiy complex, which include enclaves of Dnistersko-Buzka Series rocks, as well as intrusive and metasomatic rocks of Proskurivskiy and dyke complexes.

II-order Vinnytskiy block

It occupies the far south-eastern part of the territory and includes III-order Litynskiy block.

Litynskiy block

In the area just the north-western limb of Litynska dome-shaped structure is developed. In the gravity field Litynskiy block, also known as Gorodyshchenskiy dome, is expressed in the gravity maximum from 20 to 25 mGal in values. In the field of residual gravity anomalies the dome structure is highlighted by the number of linear arc-shaped anomalies of sub-longitudinal and north-eastern extension from 1.0-1.5 mGal in amplitude. Magnetic field includes arc-shaped linear positive Za anomalies of the north-eastern extension up to 300 nTl in amplitude. By geological-geophysical data, this part of Litynskiy block is mainly composed of enderbites, charnockites, pyroxene, magnetite-pyroxene, hornblende-pyroxene gneisses and mafic gneisses. Magnetite- bearing granulites and amphibole-pyroxene mafic gneisses are the most magnetic rocks. Enrichment of mafic gneisses in magnetite is apparently related to the processes of hypersthene mafic gneiss amphibolization and biotitization in the course of Meso-Archean charnockitization when temperatures were lower and influence of water and alkaline (potassium) components essentially higher than those of metamorphism and granitization under Paleo-Archean stage. Nature of magnetite accumulation in the leucocratic rocks (granulites) is not clear up to now. It can be assumed that these rocks comprise high-grade ancient weathering crusts developed with removal of major femic components, while residual iron was transformed in ferromagnetic [50]. Litynskiy block is the area where Meso-Archean charnockitoids are least modified in Paleo-Proterozoic, and some of these rocks (enderbite-migmatites) apparently comprise the reomorphic Paleo-Archean varieties.

II-order Berdychivskiy block

In the area just the western part of Berdychivskiy block is developed – the III-order Ivanopilskiy block.

Ivanopilskiy block

It occupies the north-eastern part of the map sheet area and is located to the north-east from Khmelnytska fault zone. In the gravity field it corresponds to the far western part of Berdychivskiy regional maximum. Gravity field intensity varies from 33 mGal (eastern map sheet border) to 22-23 mGal (north-eastern border suture of Khmilnytska tectonic zone). In the field of local gravity anomalies Ivanopilskiy block is expressed in the well-differentiated alternating ga anomalies from -1.8 to +2.0 mGal, elliptic, rarely isometric, mainly of the north-western strike. Magnetic field includes some large, extended in the north-western direction, low-gradient positive anomalies up to 2000 nTl in amplitude (Lyubarska, Malobratalivska, Kovalenkivska, Veselkivska, Lysogirska), distinguished on the background of gentle negative (up to -600 nTl), and low positive (0-150 nTl) Za field. It is revealed from the combined analysis of potential fields in Ivanopilskiy block that the highest positive (up to 2000 nTl) magnetic anomalies (Maliy Brataliv, Kovalenky, Skarzhyntsi, Lyubar villages) coincide in the space with the local ga minimums. It is known that pyroxene-bearing rocks under granitization and decomposition proceses get high magnetic susceptibility. At the same time, less intensive (0-150 nTl) magnetic anomalies (Veselkivska, to the north-east from Stetkivtsi village), that coincide with positive local gravity anomalies (up to +2.0 mGal), are caused by the weakly-altered rocks which have preserved their primary high density and low magnetization (hypersthene mafic gneisses, garnet-biotite gneisses, in places with pyroxene, graphite). After results of numeric interpretation of magnetic anomalies, the lower boundary of magnetic objects is expected to be relatively shallow (400-600 m) suggesting for deep erosion cut of the basement in this complicate elevated block.

II-order Shepetivskiy block

In the map sheet area this includes the III-order Grytsivskiy block.

Grytsivskiy block

It is located in the far north-north-western part of the territory and is bounded by tectonic breaks of Teterivska and Andrushivska fault zones. The gravity field in the western block part includes broad (up to 15 km) zone of low (up to 11 mGal) ga anomalies of north-eastern extension which correspond to Teterivska deep-seated fault zone. Further to the east the southern boundary of Grytsivskiy block follows Andrushivskiy fault and the north-east-trending fault (up to Glezne village), which can be though as the displaced fragment of Teterivska zone. In the gravity field the boundary is well expressed in the negative (-1.0, -2.0 mGal) δga linear anomalies. Magnetic field in the block includes the sites with contrasted positive anomalies up to 800 nTl in amplitude, both sub-latitudinal and north-western extension, linear and arc-shaped, consisting of individual positive anomalies from 0.5 to 2.0 km2. In the eastern block part Varvarivskiy massif of gabbro-monzonite formation is distinguished, which is expressed in high-intensity (up to 29 mGal at maximum) gravity ga anomaly, elliptic, extended over 12 km in the latitudinal direction (Kypchynskiy gravity maximum). In the field of local gravity anomalies this massif is expressed in the well-differentiated positive δga anomalies from 1.2 to 3.4 mGal, elliptic and isometric in shape, variously oriented. Magnetic field is negative in general (up to -550 nTl) and in the central part only (in the western half) the biggest, extended over 10 km in the sub-latitudinal north-western direction (hockey-stick in shape) positive Za anomaly is distinguished, from 250 to 500 m wide and up to 170 nTl in amplitude. The western, most extensive part of the anomaly, exhibits higher Za gradients than the eastern one which is less prominent. Geological nature of Varvarivskiy massif and its envelope was adjusted in the course of EGSF-200 by drilling data of DH 32, which at the depth 29.8 m had encountered gabbro-monzonite with density 2.82 g/cm3 -6 and magnetic susceptibility 712×4π×10 CI units. The same rocks were also intersected in DH 18886 (σavg. = 2.84 g/cm3, æ = 300×4π×10-6 CI units), drilled in Kypchynska magnetic anomaly. In the southern part of Kypchynska positive gravity anomaly, in the outcrops 59-61, the garnet-biotite migmatites and gneisses are 3 -6 intersected (σavg. = 2.73 g/cm , æ = 40÷50×4π×10 CI units), and in the outcrop 58, located at the epicenter of local gravity maximum – garnet-biotite migmatites and amphibole-biotite gneisses, obviously formed after mafic 3 -6 rocks (σavg. = 2.81÷2.91 g/cm , æ = 63÷168×4π×10 CI units). Geological structure of the map sheet M-35-XXII is complicated by numerous tectonic breaks. Below description of the major ones is given.

66Tectonic breaks

Khmilnytska fault zone

In the map sheet M-35-XXII Khmiltynska tectonic zone comprises the major disjunctive break which essentially defines tectonic features both in the basement and overlaying sedimentary units. The zone crosses map sheet territory from the south-east (from Khmilnyk town) to north-west with two branches (south-western and north-eastern), which are abruptly limited by the breaks of Teterivska and Andrushivska fault zones. In general, both branches of Khmilnytska zone are observed in sub-parallel fashion in 8-12 km from the eastern map sheet border, and then the fault of Bilokorovytska zone move up the lineaments of the north-eastern branch with amplitude up to 2-4 km, whereas faults of Ostropilska zone break and move up the south-western branch by the distance up to 15 km. The north-eastern branch of Khmilnytskiy fault is traces in the map sheet limits over 35-40 km at the width 4-5 km. The south-western branch crosses entire map sheet almost by diagonal and is traced over the distance of 70-75 km; in the southern part it is 9-10 km wide and just after the cut by the fragment of Ostropilskiy fault the width drops down to 3 km. After the crossing of Khmilnytska zone by Teterivskiy fault the first one does actually pinch out and is only conventionally traced by some local gravity anomalies of the north-western extension.

98 In general, Khmilnytska zone is confidently distinguished by geophysical data. In the gravity field it is expressed in the chains of low ga gravity values (10-17 mGal). The boundaries of Khmilnytska tectonic zone are clearly expressed in the high (up to 30 eotvos per km) horizontal gravity gradients. In the field of local gravity anomalies Khmilnytska tectonic zone is mainly expressed in the linear negative anomalies δga. The biggest in size δga anomalies are located close to Khmilnyk town, Skarzhyntsi, Maryanivka, Bycheva, Pyshky, Onankivtsi, Brazhyntsi and other villages. The bulk gravity effect is caused by several factors: increased thickness of less dense sediments in depression and occurrence of low-density leucocratic granitoids of Khmilnytskiy complex in the basement. The crystalline rocks in the fault zone are highly cataclased and milonitized, often silicified, graphitized and sulphidized. Positive residual anomalies δga (0.7-1.0 mGal) in the zone are mainly caused by garnet-biotite gneisses and, probably, the mafic rock bodies not exposed by erosion. Magnetic field in Khmilnytska fault zone is also complex. On the background of gentle Za field -100…- 700 nTl in amplitude a range of positive anomalies of various shapes and sizes are observed: from isometric up to 200 m in diameter, for example, nearby Zhdanivka village, to linear, up to 2-14 km long ones. The biggest is size anomalies are distinguished close to Skarzhyntsi, Maryanivka, Bycheva, Ostropil, Gizivshchyna and other villages. These anomalies are confined to the fields of regional gravity maximums and caused by occurrence of the large massifs of Lithynskiy complex charnockitoids. In the junction node of Khmilnytska and Bilokorovytska tectonic zones Khmilnytskiy gravity minimum is distinguished; its central part is located to the south from Khmilnyk town, close to Stara Guta village. The minimum is sub-isometric and slightly elongated in the north-north-western direction (Fig. 5.1). In the transformed gravity field the zone is expressed as the site of lowest gravity values with some local minimums. Magnetic field is also negative. Geological-geophysical model of the gravity minimum corresponds to the large mushroom-shaped granitoid massif, whose upper part (at the level of crystalline basement section) attains 20-25 km in diameter, while the central “leg” plunges down to the depth 7 km. The central part of the massif, in our mind, is complicated by the minor granitoid body of irregular asymmetric shape with average density 2.58 g/cm3. In the plane this body is sub-isometric, 5 km in diameter, with the lower boundary depth about 3 km. The most leucocratic granite varieties are developed therein. After detailed gravimetric survey and drilling data, Khmilnytskiy massif is complicated by minor remnants of garnet-biotite granites and this may suggest for the later time of Khmilnytski granite formation in comparison with granitoids of Berdychivskiy complex. Zhdanivskiy massif of ultramafic rocks with secondary hydrothermal-metasomatic alteration of crystalline rocks (albitization and biotitization) is confined to the junction of Khmilnytska and Bilokorovytska zones.

Khmelnytska fault zone

This one crosses entire map sheet from the western to eastern borders and is traced over the distance of 72 km. Zone thickness (by geophysical data) attains 20-22 km. The far southern fault follows the line of villages Pyrogivtsi-Goloskiv-Dyakivtsi although some fragments of sub-latitudinal breaks are also observed to the south. Most extensively tectonic breaks are expressed in the central part of this zone, in between Davydkivtsi and Antonivka villages in the north, and Kopystyn – Maydan-Verbetskiy in the south. The far northern fault (the border between Medzhybizkiy and Veselivskiy blocks) of Khmelnytska tectonic zone follows the line of villages Veselivka – Pylyavka, where it is crossed by Letychivska fault zone, and then it is developed in the fragments from Ivankivtsi to Kumanivtsi villages. Khmelnytska tectonic zone in the gravity and magnetic fields is expressed in the zones of maximum module values of horizontal gradient, in the linear minimums, alternating fields, and in the broken correlation between the anomaly axes. The fault zone is confidently expressed in the satellite images. Over entire length it is accompanied by the linear weathering crusts. The faults of Khmelnytska tectonic zone, especially at its cross- junction with Letychivska zone, were formerly the channels for Proskurivskiy complex intrusions.

Bilokorovytska tectonic zone

It is expressed in the fragments in the far eastern map sheet part, where crosses it out from the north to south. In the gravity field it is expressed in the broad (from 9 to 14 km) ga minimum (from 6 to 19 mGal). As noted before, Khmilnytskiy gravity minimum is confined to the cross-junction of the given zone with Khmilnytska one.

Khmilnyk town

A B

g a observed 3.0 mGal

g a fitted

A B 35 40 45 50 55 60 L, km 0 W 0.07 E -1 2.65 -0.03 -2 2.58 -0.15 -3 2.61 -4 -5 0 0 2.76 -6 2.76 -7

H, km

0.07 123456 2.65

Fig. 5.1. Density model of Khmilnytskiy gravity minimum.

1 – density values of host rocks: in numerator – surplus; in denominator – absolute; 2 – Berdychivski 3 3 garnet-biotite granites and migmatites (σavg. = 2.76 g/cm ); 3 – biotite, garnet-biotite granites (σavg. = 2.65 g/cm ); 3 4 – biotite, aplite-pegmatoid granites (σavg. = 2.61 g/cm ); 5 – leucocratic aplite-pegmatoid granites (σavg. = 2.58 g/cm3); 6 – contour of leucocratic granite massif.

100

Magnetic field in general is negative, complicated by positive linear Za anomalies 100-300 nTl in amplitude, caused in the southern part by pyroxene, hornblende-pyroxene gneisses and mafic gneisses and diabase dykes, and in the northern part also by magnetite-bearing charnockitoids (western part of Ivanpilskiy block). In the southern part Bilokorovytska zone is complicated by the faults of Khmelnytska zone, and in the central part – by Ostropilska zone and the fragments of Ulanivska synform structure; the far western part of the latter enters the map sheet from the east over the distance of 5-6 km.

Andrushivska tectonic zone

It is discontinuously observed in the northern part of the area in sub-latitudinal direction from Verbkivtsi village in the west to Glezne village in the east, where it is crossed by Lyubarskiy fault (one of the branches of Teterivska deep-seated fault zone), and then conventionally to the east up to the map sheet border. Most confidently it is traced in the western half of the area, where it is expressed in the clear linear ga field minimums up to 12 mGal in amplitude, located just nearby the anomalies above Varvarivskiy massif. In our opinion, in the section of Andrushivska zone in between Sasanivka and Glezne villages the Teterivska fault zone is displaced in the western direction, and the northern border of Dnistersko-Buzkiy mega- block is located. To the east from Glezne village just the fragments of Andrushivska fault zone are distinguished by the sharp changes of ga field isoanomal strike and increased values of the horizontal gradient values. This is caused by the cross-junction of the zone with Bilokorovytska tectonic zone. In the outcrops nearby Yurivka village the cataclasites, milonites and even ultra-milonites are widely developed in the zone. Andrushivska tectonic zone is also distinguished by the satellite image data. It is well expressed in the modern relief and in the relief of crystalline basement surface by the occurrence of linear paleo-valleys and thick (up to 16 km) weathering crusts [44].

Letychivska tectonic zone

The zone crosses entire studied area from the south-east, from Biletske village to the north-west to Starokostyantyniv town and further up to Teterivska tectonic zone, over the distance 62 km, being 3-8 km wide in the southern part. In the gravity field the zone is expressed by the chain of gravity minimums and highest values of the horizontal gradient module ga, and in magnetic field – by negative Za (Ta) values. In the relief of crystalline basement the zone corresponds to Letychivska linear depression with altitudes from 220 to 240 m distinguished at the watershed of South Boug and Ikva rivers. In the fragments the zone is also traced after satellite images. Over almost entire zone length the linear weathering crusts are developed. Previous authors [51] had distinguished Kopachivskiy, Rudnyanskiy, Letychivskiy and Romanivskiy faults in the zone which are most expressed in geophysical fields. Kopachivskiy fault apparently comprises the far south-western break of Letychivska zone. It is observed over the distance of 12 km in the band 400-700 m wide where drop of magnetic properties and rock decomposition are noted. To the south (in “Bar” map sheet) the low-amplitude polarization anomalies are related to this fault, characteristic for sulphide mineralization, and also mercury-metric anomalies, that allowed previous authors [V.A.Entin, 1994] ascription of Kopachivskiy fault to the zones of young activization and tectono-magmatic re- working. In the area of Pyrogivtsi village the fault is cut by Khmelnytska tectonic zone and further to the north some fragments only are conveniently distinguished. Rudnyanskiy fault is traced from the southern map sheet border (Terlivka village) to the northern boundary of Khmelnytska tectonic zone, crossing the latter nearby Yaroslavka village. In the gravity field the fault is expressed in the zones of high gradients and linear gravity minimums. It is also distinguished after satellite image data processing. In the southern part the fault is accompanied by the linear weathering crusts [51]. The alkaline and sub-alkaline rocks of Rudnyanskiy massif are confined to the cross-junction node of Rudnyanskiy fault with the breaks of north-eastern and sub-latitudinal extension. Letychivskiy fault (the central one in the same-named zone) is extended over the distance more than 60 km from the southern map sheet border up to Teterivska tectonic zone. In the gravity field the fault is expressed by linear minimums, high horizontal gradient zones, and in changes of the anomaly axes direction. Some fragments are supported by the satellite image processing data, as well as by development of linear weathering crusts.

101 Romanivskiy fault, like Letychivskiy one, is confidently traced from the southern map sheet border up to Teterivska zone but in the southern part it is complicated by sub-latitudinal shears along Khmelnytska zone. Romanivskiy fault is expressed in the high gradient zones and linear local gravity minimums, as well as in the sharp change of isoline direction, local minimums and magnetic field gradient zones. The syenite bodies of Verbkivska site and alkaline mafic-ultramafic rocks of Antonivskiy massif are confined to the cross-junction zones of Romanivskiy fault and faults of Khmelnytska zone. Romanivskiy fault apparently comprises the far north-eastern suture of Letychivska fault zone.

Teterivska deep-seated fault zone

This zone crosses the map sheet in its far north-western part over the distance of 30 km. Observed thickness of the zone in the map sheet limits is up to 15 km. The gravity field of Teterivska tectonic zone comprises the broad (up to 20 km, including 15 km in the studied area) zone of low (up to 11 mGal) ga field anomalies. Gravity field intensity over there is comparable with that of Khmilnytskiy gravity minimum. However, in contrast to the latter, Teterivska tectonic zone in the field of local gravity anomalies is not expressed indicating much greater (10 km and more) depth of the zone. In Teterivska tectonic zone contrasted area of positive linear sub-latitudinal magnetic anomalies up to 5 km wide and up to 800 nTl in amplitude is distinguished. This Ta area is caused by the occurrence of granodiorite rocks in the upper column part (up to 300-400 m). In the opinion of many authors, Teterivska zone comprises the boundary between Volynskiy and Dnistersko-Buzkiy mega-blocks. It is also supported by the EGSF-200 data. No rocks of Vasylivska Suite of Teterivska Series, characteristic for Volynskiy block, are observed to the south-east from the marginal fault of this zone, and granitoids of Sheremetivskiy and Zhytomyrskiy complexes are also not encountered therein.

33Upper tectonic level

The upper tectonic level consists of the sedimentary cover rocks, including Vendian, Mesozoic and Cenozoic, which discontinuously overlie the lover level, filling up depressions in the crystalline basement. In the upper level three tectonic floors are distinguished: Late Precambrian (Vendian), Mesozoic and Cenozoic. In turn, Cenozoic tectonic floor consists of three tectonic sub-floors: Paleogene, Neogene and Quaternary ones.

67Vendian tectonic floor

According to the common tectonic zonation, the map sheet territory is located in the junction zone of Ukrainian Shield and Volyno-Podilska plate. The western boundary of Ukrainian Shield, according to the decision of Inter-ministry Stratigraphic Committee, is set by the boundary of Vendian sediments, and the area of relatively shallow depth of the crystalline basement surface, which gently and gradually plunges down in the west-south-western direction, is considered as the separate tectonic unit – the western slope of Ukrainian Shield. Previous authors had commonly thought that boundary between the Shield and its slope is of tectonic nature. Koretskiy fault, distinguished by N.E.Strelkova [54] as the structure by which the boundary is set between the Shield and its slope, is not distinguished as the regional-scale break according to the recent data, geophysical first of all. In the western slope and adjacent Shield portion the local sub-longitudinal breaks are developed providing “keyboard” or small-block structure of the basement and Vendian rocks. Apparently most mentioned faults were established in pre-Riphean times and some of these breaks were then activated in Vendian and later. Monocline dipping of Vendian sediments indicates gradual plunging of the Volyno-Podilska plate basement. Thus, the boundary between the Shield and its slope is of erosion-tectonic nature. In the studied area the Vendian rocks are developed over monocline composed of rhythmic intercalation of the clay and clastic rock batches, which are distinguished as the litho-stratigraphic units. The monocline gently plunges down in the western and south-western directions. Rock dipping angles vary from 1-2o in the eastern part to 4-6o in the western. Respective increasing of their thickness is observed with the rate from 2-3 to 6-8 m per kilometer. At the sites with considerable erosion-tectonic cutting of the crystalline basement surface irregular changes in the thickness of Vendian sediments are observed. Their tight relations with hypsometry of basement surface are also evidenced by the curvilinear, wavy boundary of their modern distribution. The rhythmic intercalation of the strike-persistent Vendian litho-stratigraphic units of different composition had caused morphology of their exposure at pre-Mesozoic surface, and in places where Mesozoic

102 sediments are absent – at pre-Cenozoic surface. At this surface Vendian sediments are observed in sub- longitudinal bands of various widths, sequentially replacing one another in the west-south-western direction, adding up the column. The band boundaries are slightly-wavy and apparently reflect tectonic bends. Analysis of regional distribution of Vendian sediments, specifically, sub-units mapped in the map sheet M-35-XXII, allows two rock complexes distinguishing with different tectonic patterns – Volynskiy and Mogyliv-Podilskiy sub-floors. The lower one, Volynskiy sub-floor composed of mainly volcanogenic rocks, is of the north-western strike. The upper, Mogyliv-Podilskiy sub-floor, mainly terrigenous in composition, is of sub-longitudinal strike. The boundary between the two is marked by the basal horizon of Olchedaivski sandstones occurring at the bottom of the upper sub-floor. In the studied area the faults in Vendian sediments are not encountered by direct observations but the fault-block structure of this tectonic floor can be supported by the following indirect evidences: - relief patterns of pre-Mesozoic – pre-Cenozoic surface and, specifically, Vendian surface; - spatial variability of Vendian sediments thickness; - tectonic control of litho-facies changes in Volynska Series columns; - tectonic features of the overlaying tectonic floor; - spatial relations of the modern river network with the basement and Vendian structures. The surface relief of the Vendian units is developed under influence of erosion and tectonic factors. Since Vendian rocks include the varieties of different density and susceptibility to erosion, the highest relief altitudes are related to the exposures of sandstones, specifically, ones of Olchedaivski layers. These exposures are also observed in the broadest fields. On the background of general relief ascending in the southern direction, its relatively uplifted and subsided sites of clear north-western extension are observed (Fig. 5.2). Two of these, in the southern part of map sheet, coincide with the South Boug and Buzhok river valleys. They correspond to the contrasted changes in the crystalline basement surface hypsometry and, as a result, essential variability in thickness of Vendian sediments (see Fig. 5.2). In the north of the area depressions in the basement relief are also reflected in the depressions of pre-Mesozoic relief (Butivtsi, Zelentsi villages) filled with Khomorski sediments of increased thickness. The Vendian sediment thickness variability in the studied area, and in more extent in the territory adjacent from the west, suggests for tectonic control from the diagonal system of tectonic breaks. On the background of general thickness rising in the north-western direction, some north-east-trending zones with tightened isopachs are observed, indicating stair-like mode of thickness increasing. At the same time, the west-trending sites alternate with relatively decreased and increased Vendian thicknesses. Apparently thickness variability of Vendian sediments is related to the basement block motions. The zone of transitional column types of Volynska Series, where volcanogenic rocks are gradually substituted by mainly terrigenous clastic sediments, is extended in the south-western direction. The link between the modern river network in the territory, at least in its south-western part, and the Vendian tectonic plane is evidenced by the structure of South Boug river valley. Being linear over significant distance, starting from the upper courses, the valley morphology in the studied area is complicated by the sharp bend which coincides with the Vendian sediments “tongue” extended towards Ukrainian Shield, in the direction of Goloskiv village. Perhaps, the modern river valley shape is related to the activization of tectonic break which had affected sedimentation of Vendian time.

68Mesozoic tectonic floor

Mesozoic tectonic floor with angular and stratigraphic unconformity overlies Vendian tectonic floor. It is composed of Cretaceous sediments which gently monoclinally plunge down in the western direction. Spatially the rocks of Mesozoic tectonic floor are confined to the western slope of Ukrainian Shield. The faults in Mesozoic tectonic floor are low-amplitude, mainly extended in the sub-latitudinal and north-western directions and partly control erosion sites of Cretaceous sediments. In general, ascending of pre- Cretaceous surface in the southern direction is observed in the map sheet. After results of morpho-structure analysis, the south-western part of the area (Khmelnytska morpho- structure) underwent descending motions under neo-tectonic stage. This can explain why the footwall inclination of Mesozoic (and Paleogene) rocks in the area is changed from the western direction to southern one.

69Cenozoic tectonic floor

Cenozoic tectonic floor is developed throughout the map sheet area and composed of Paleogene and Neogene marine and continental rocks and Quaternary sediments of various genetic types. Cretaceous sea regression is related to the active phase of initial Alpine tectogenesis, and then until beginning of Middle Eocene the territory had comprised the elevated land.

103

101 1787 222.0

222.6 2 1 20 228 17761776 219.1 383 234.0 221.0 40 223.0 3 225 227.4 25 2 20 425 2 438 232.0 178 225.0 215.3 303 304 2 4 230.0 2 0 245.0 351 18 2 30 2 2 231 230.0 1 0 302 177 0 235.0 207.3 230 124 445 219.4 225.0 408 18240 441 234.0 248.0 228.0586 241.3 590 245 242.5 8 2 241.5 35 Starokostyantyniv 9 10 238.5 232.8

109 582 2 250256.0 246.0 24 331 5 240.0 240 24 5 567 310 172 245.0 245.0 239.9 30 19 505 240.3 244.0 239.0 240 235 230 225 18226 220 247.9

112 5 107 4 218.6 2 248.0

17 130 238.7 244.5 240 245 308 12 240.1 244.2 18239 236.5

5 2 46 0 5 247.9 543 2 248.0 116 90 238.5 259.5 291 25 243.1 5 250 15 741 245 244.5 18237 249.2 244.1

0 240 5 5 309 2 4 2034 2 248.5 249.9 245 18238 129 255.3 231.0

1:500 000 5 kilometers in 1 centimeter 50 10 20 25 km

Relief scale (m)

200 210 220 230 240 250 260

40 1 309 2 3 2 248.5 4

Fig. 5.2. Map of Vendian surface relief.

1 – isohypses of Vendian surface relief; 2 - drill-holes intersected Vendian rocks: in numerator – drill- hole number, in denominator – Vendian surface altitude; 3 – Vendian eastern boundary; 4 – probable tectonic breaks.

104 Structure of Paleogene and Neogene tectonic sub-floors in the area is distinct in the north-eastern part making possible distinguishing of two LTZs: Berdychivska and Khmelnytska. The boundary between the two is controlled by activated at that time Khmilnytska tectonic zone of the north-western extension. While Paleogene and lower part of Neogene sub-floors are spatially separated, at the level of Upper Miocene and Pliocene they are combined and clear boundary between these LTZs is not observed. In the north-eastern part of territory, in Berdychivska LTZ, activization of Khmilnytska tectonic zone is accompanied by development of erosion-tectonic paleo-valleys and their major direction is controlled by the north-western faults. In the erosion paleo-valleys-depressions the continental Buchatski sediments were depositing in the beginning of Middle Eocene. In the western slope of Ukrainian Shield the territory underwent considerable subsidence in Kyivskiy time reflected in more deep-water facies sediments. The eastern boundary of Kyivska Suite in general coincides with the boundary of Cretaceous and Vendian rocks. In Obukhivskiy time descending motions continued predominate but with the trend for progressive ceasing and periodically were changed by ascending motions. At the end of Eocene new stage of tectonic activation was accompanied by ascending motions over entire territory with pre-Miocene smoothing surface development. Tectonic motions in Neogene were oscillating. The fault activation in pre-Sarmatian time was resulted in the dimples on the crystalline basement surface and ancient hydro-network development. In the Early-Middle Miocene time Poltavske sea-lake had been transgressed into the far north-eastern part of the territory (Berdychivska LTZ) from Dniprovsko-Donetska Depression through the central part of Ukrainian Shield. In this basin Novopetrivska Suite sediments were depositing, which are preserved from erosion in the dimples of crystalline basement surface. In Middle Miocene time the waters from southern basin had entered the far southern part of the area (Khmelnytska LTZ), apparently because of subsidence in Khmelnytska fault zone. The shallow-water sediments of Podilska Suite were depositing over there. In Early Sarmatian time the sea had transgressed over most part of the territory, except the north-east, following depressions in the crystalline basement relief. Tectonic regime instability at this stage was expressed in the low-amplitude motions reflected in the lens-like clay and marl interbeds in limestones at relatively elevated sites. In Middle Sarmatian descending was changed by uplifting accompanied by oscillating motions, reflected in the lens-like limestone sediments in clayey-sandy sediments. Middle Sarmatian sea, expanding from the south-west to north-east, was shallow-water. In the coastal sea part (tidal-flat zone) organogenic limestones were depositing. In Late Miocene and Pliocene entire territory of Khmelnytska LTZ had comprised the area of steady uplift resulted in denudation processes reflected in the partial lacking of respective sediments therein. Berdychivska LTZ at that time was apparently more stable in tectonic respect and the sequences of parti-colored and red-brown clays were depositing over there. Development of Quaternary tectonic sub-floor is caused by notable ascending epeirogenic motions and activation of sub-latitudinal and north-western faults. On the background of general uplift differentiated block motions of various intensities and strikes had occurred. More extensive uplift in the western part of territory had caused reverse relief development and extensive erosion processes, as well as lowest thickness of Quaternary cover in Khmelnytskiy, Ikopotskiy and Trebukhivskiy areas. Stable tectonic regime in Litynskiy area had preserved highest thicknesses of Quaternary sediments. Activation of some fragments of tectonic breaks is expressed in the arc-shaped and bend-like turns of river valleys. These are most notable in the river valleys of South Boug (Goloskiv, Popivtsi and other villages), Sluch and Ikva (Stara Synyava village). Block motion differentiation is expressed in alternating broad swamped and narrow flood-lands, in places with rapids and benches, in the river courses of South Boug (in between Novokostyantyniv and Guli villages) and Sluch (Korzhivka-Gubin villages). After results of morpho-structure analysis, the system of linear, linear-planar and planar morpho- structures is distinguished in the modern tectonic plane of the territory. Of the planar ones, the block and central morpho-structure types are distinguished. The complex block structure is caused by interaction and crossing of linear, arc and ring faults. The linear morpho-structures in the area are mostly sub-latitudinal and diagonal. Sub- longitudinal directions in morpho-structure respect are recessive and weakly expressed, except Staroostropilska linear-planar morpho-structure. Apparently this indicates the modern re-arrangement of tectonic plane in the area. The west-north-western zones, mainly transitional, are regularly distributed over entire studied area. The distance between these zones varies from 6 to 10 km. They are traced almost over entire length with minor interruptions.

105 The north-eastern fault zones are less regularly distributed and interrupted by sub-latitudinal faults. The distance between these zones is 10-12 km. The linear morpho-structures, oriented in the north-north-western direction, are not arranged in the long bands and developed mainly in the western part of the territory. The fault zones of north-western direction are irregularly distributed over the territory. The distance in between is from 2 to 9-10 km. They discontinuously follow Letychivska zone and the north-western and north- eastern branches of Khmilnytska tectonic zone. Sub-latitudinal fault zones are mainly developed in the northern and southern parts of the territory. By geophysical data they correspond to the regional tectonic zones. The northern zone is more clearly expressed in erosion forms (Derevychka river, terrace benches of Khomora river). The southern zone is developed in some fragments along the river valleys of South Boug, Buger, unnamed branch of Khavos, Kudyma (Grechyntsi- Rozhny villages). In the central part of map sheet sub-latitudinal zone is discontinuously expressed in the Sluch river valley, and the major watershed of Sluch and South Boug rivers. Important role in morpho-structure of the territory is played by the system of diverse-rank central-type morpho-structures (CMS). After morpho-structure analysis, in the map sheet M-35-XXII two trans-continental CMS contours are distinguished – Mediterranean and Dniprovo-Volzko-Baltiyska, as well as trans-regional – Prypyatska, I-order regional – Zhytomyrska, II-order regional – Dnistersko-Buzka. In the map sheet area two III- order regional CMS are defined – Khmilnytska and Sluch-Pivdennobuzka, as well as 16 local I-III-order CMSs. Thus, the modern tectonic plane, developed over neo-tectonic stage, is expressed in the modern relief and related to the general territory uplift and activation of tectonic breaks.

106

76. HISTORY OF GEOLOGICAL DEVELOPMENT

In the geological history of the territory two major stages are distinguished: pre-Vendian – development of crystalline basement, and Vendian-Phanerozoic – development of sedimentary cover.

34Archean-Proterozoic stage

The oldest (3600-3500 Ma) [9] rocks in the area constitute litho-tectonic complexes developed in geodynamic environments of primary proto-crust formation and composed of granulite-basite, kinzigite and enderbite-migmatite formations.

70Paleo-Archean epoch

Paleo-Archean is characterized by extensive magmatic activity: initial volcanism with thick basalt flows and co-magmatic mafic-ultramafic minor intrusions. Analysis of volcanism and sedimentation conditions in Early Precambrian [5] indicates high probability of hydrosphere with water temperature about 70-100oC. Atmospheric conditions have included high concentration of volcanic gases and reactive properties when thick enough sedimentary sequences were able to form under leading role of chemical dissolution. Their deposition had accompanied by volcanic eruptions. Because of low thickness of crustal rocks and significant heating at the depth, ascending mantle high- temperature heat flows had caused rock metamorphism under granulite facies conditions. The earliest of the studied in the area meta-basalts of Tyvrivska sequence and meta-mafic-ultramafic rocks of Sabarivskiy complex constitute granulite-basite formation, and the rocks of Bereznynska sequence – kinzigite formation. At the boundary of 3400 Ma meta-volcanogenic and meta-volcanogenic-sedimentary rocks were plagiogranitized under granulite facies conditions. Granitization products – Gayvoronskiy complex gneiss-like enderbites of tonalite composition – constitute the enderbite-migmatite formation. Thus, by the end of Paleo- Archean the thick and rigid enough proto-crust was developed in Podilskiy micro-continent, and the biggest and least-altered fragments of this crust are noted in Medzhybizka and probably Litynska dome structures. The folding at this stage had included enderbite-gneiss domes and arc-shaped systems of very tight (up to isocline) folds in around the domes, and bigger synforms in between the domes. The latter are normally filled with kinzigites. Distinctly, there are no younger supra-crustal rocks in the given area as the part of Podilskiy block. Further geodynamic regime was defined by periodically appeared collision environments related to the geological processes in adjacent regions of Ukrainian Shield.

71Meso-Archean epoch

At the boundary of Meso- and Neo-Archean, in relation to the riftogenic processes in adjacent Rosynsko-Buzka litho-tectonic poly-zone, collision environment establishing (early collision) was probably caused by the horizontal crust displacement during rift extension. Charnockitoid formation of Litynskiy complex is related to this environment. At the early stage the massifs of Paleo-Archean enderbites were retrograded and partly remobilized; under rising potassium activity these rocks were modified to leuco-enderbites and then charnockites (charnockite formation). Metamorphic rocks of Dnistersko-Buzka Series also underwent charnockitization. In the eastern part of the area Litynskiy dome was developing as the steady antiform structure and Medzhybizkiy dome was remobilized; in the central and northern parts the minor dome structures with charnockitoids in the cores were developed. Probably at that time the major north-western faults were established which separate Litynskiy and Medzhybizkiy domes – Romanivskiy, Letychivskiy and Rudnyanskiy, as well as Khmelnytska tectonic zone and major sub-longitudinal break in the western part of Litynska structure – Bilokorovytsko-Yablunivska tectonic zone. Activity of these breaks had affected partial re-arrangement of tectonic plane in the area: together with the fold-dome structures the linear folds of mainly north-western extension were developing. Mentioned conditions and respective geological formations of Podilska LTZ were probably characteristic also for Volynska LTZ.

107 72Neo-Archean – Paleo-Proterozoic epoch

At the boundary of Neo-Archean and Paleo-Proterozoic, in Volynska LTZ the granulite crust by the fault systems of the north-eastern (Teterivska zone) and sub-latitudinal (Andrushivska zone) directions was buried and above, in the litho-tectonic paleo-zone of continental rifts and related minor basins, development of terrigenous-volcanogenic formation (Vasylivska Suite) had commenced. At about 2430 Ma the rocks of Vasylivska Suite underwent plagio-granitization with development of tonalites and plagio-granites of Sheremetivskiy complex, probably, in relation to the early, partial and intermediate collisions of the given basin. Further evolution of paleo-rift into large basin was accompanied by the development of upper part of Teterivska Series to the north of the studied area. The marginal part of Volynska LTZ, adjacent to Podilskiy micro- continent, was developing under conditions of active continental margin. The magmatic arc, characteristic for these environments, had emerged over there with intrusions of gabbro-monzonite formation (Bukynskiy complex), represented in the studied area by Varvarivskiy massif and its satellites.

73Paleo-Proterozoic epoch

Further transformations of Podilska LTZ basement and Vasylivska Suite rocks were related to the collision processes of Paleo-Proterozoic basins (Volynskiy and Ingulskiy), encompassed entire western part of Ukrainian Shield and accompanied by most extensive ultra-metamorphic granitization. Granitoids of Berdychivskiy complex (kinzigite-granite formation) in their compositional variability exhibit clear links with substratum and are autochthonous. The latest only leucocratic and pegmatoid granites of this complex display allochthonous evidences. As a result of Early Proterozoic granitization, mature continental crust was established over entire territory. Both crustal composition (up to 70% of the upper horizons are composed of kinzigite-granite formation) and tectonic plane of the territory, except most steady blocks of earliest consolidation, underwent essential modifications. Paleo-Proterozoic domes contain granitoids of Berdychivskiy complex in the central parts. The older charnockitoids and supra-crustal rocks were pushed off to the dome periphery and more or less underwent regional K-feldsparization. Due to various stage folding and granitization overprinting, the fields of supra-crustal rocks get complex irregular shape. Tectonic plane complication is also related to the emerged brittle faults of the north-western and sub-latitudinal strike. In Volynskiy mega-block collision processes and granitization led to the development of two-mica Zhytomyrski granitoids which belong to granite-migmatite formation of late-collision geodynamic environments. In Podilskiy block at the end of Early Proterozoic, in relation to the emerged rigid crust above the mantle heated over previous collision phase, in the basalt layer or at the boundary between the basalt and peridotite layer, incipient melting zones had appeared. The melt transport form these zones in the minor stock- like or fissure intrusions had occurred in the crustal breaking zone by the system of sub-latitudinal faults of Khmelnytska tectonic zone. In the zone, intrusions are concentrated in three separate fields (Antonivske, Rudnyanske and Goloskivske). Large enough massifs exhibit diversity in rock composition and layering, highlighting their multi-phase nature and degree of metasomatic re-crystallization. Fissure intrusions are simpler in structure. The bodies constitute alkali-gabbroid formation with the natural range gabbro – essexites – ijolites – nepheline syenites – syenites – phenites, developed in the geodynamic environments of internal plates, in the litho-tectonic paleo-zone of hot spots and lines. The rocks in formation are enriched in apatite with highest contents in alkaline mafic and mafic members of the range. The final stage of late collision is expressed in activization of the major north-west-trending tectonic structure – Khmilnytska tectonic zone, which had separated II-order Berdychivskiy and Khmelnytskiy blocks. In the zone the allochthonous massifs and vein bodies of leucogranite formation were intruded (Khmilnytskiy complex), and extensive processes of the host rock hydrothermal-metasomatic and tectonic re-working developed. The faults were also activated outside Khmilnytska zone (mainly north-western and sub-latitudinal) where microclinization, silicification and sulphidization had been developed. Subsequent stages of Khmilnytska zone activization include Zhdanivskiy ultramafic massif (1850 Ma) and the north-west-trending and sub-latitudinal diabase dykes (about 1700 Ma). In the zones of activated faults, comprised migration channels for low-temperature hydrothermal solutions, the early high-temperature mineral assemblages were replaced by chlorite, epidote, carbonate, and brittle tectonic deformation sealing with these minerals. In further epochs tectonic activity of crystalline basement was expressed in the block motions of different orders and amplitudes, which together with exogenic factors had affected weathering crust formation, as well as structure of the sedimentary cover.

108 The sedimentary cover composed of Vendian, Mesozoic and Cenozoic rocks, occurring with sharp angular unconformity over the crystalline basement rocks and their weathering crust, was developing in several stages related to different tectonic regimes, paleo-geographic and paleo-climatic environments, which essentially differ for various parts of the studied area.

35Vendian stage

The geological history of studied area in Late Precambrian time had been determined by evolution of two paleo-structures – Volyno-Poliskiy trough (VPT) and Podilskiy uplift of Ukrainian Shield, since the given territory is located in between these two. Tectonic plane of Volyno-Podilska margin of Eastern-European platform (EEP), and specifically the studied area, was established as far back as Early Proterozoic and included the system of deep-seated faults of north-eastern and north-western extension, which affected development of sedimentary cover in Late Precambrian (Riphean, Vendian). The VPT emerged as the south-western extension of the system of deep depressions and rifts that split EEP in Riphean and became the zones of extensive sedimentation. Their establishing is related to Early Baikalian phase of tectogenesis where the geosyncline regions were involved along the platform periphery. The studied are is located on the south-eastern slope of this paleo-structure. During Middle and Late Riphean the rocks of Poliska Series were depositing in the intra-continental basin that covered VPT and outside its margins being extended eastward up to Ovrutska depression and involving the marginal parts of Volynskiy and Podilskiy blocks of Ukrainian Shield. At the end of Riphean, due to the VPT bottom and south-eastern envelope uplift, the rocks of Poliska Series were elevated to the surface and get eroded. Their modern boundary is located in 20 km to the south-west from studied area, in the area of Izyaslav town. At the boundary of Riphean and Vendian the sharp change in climatic conditions had happened, from dry arid to the wetter but colder ones. At the beginning of Vendian the VPT underwent some subsidence resulted in the expansion of water basin existed since Late Riphean therein. The distinct sediments were depositing in the basin – tillites (conglomerate-breccia, unsorted sandstones etc.), which contain not only local rock fragments but also exotic ones brought from afar. This gives reasons for the rock ascription to the glacier sediments. Tillites are mapped nearby the north-western map sheet corner in Brodivska Suite. During Riphean and beginning of Vendian the studied area was kept relatively elevated and no sedimentation evidences are found. The crystalline basement underwent destruction due to fault activation related to the tectonic movements in adjacent VPT. The weathering processes predominated over that time, being more extensive in the crushing zones. Probably, the south-western part of the area, as the part of Podilskiy uplift of Ukrainian Shield, ever since that time had occupied relatively higher hypsometric position and got extensively eroded. In Volynskiy time the VPT underwent further subsidence and expansion. The water basin covers the north-western part of the area where Khomorski layers were depositing under coastal shallow-water conditions complicated by depressions. Lithology of these layers (rounding, composition) indicates their actually local eluvial-deluvial origin, specifically this concerns the basal breccia. Khomorski layers had smoothed eroded basement surface filling up all irregularities including those of tectonic nature. In the far eastern field of their distribution the kaolineous arkosic sandstones were deposited which may suggest for the erosion of weathering crusts of respective composition. The north-west-trending fault activation in the axial zone of VPT in post-Khomorskiy time had stimulated appearance of volcanic centers and development of so called trapp (flood-basalt) formation of Volynska Series. At the initial phase of this formation the extrusive-pyroclastic rocks were formed (Zabolotivska Suite), which are not known in the studied area and mapped to the west from Lutsk town. At the middle phase (Babynskiy time) volcanic activity becomes mainly explosive and resulted in the thick pyroclastic sequence that covered significant squares including the north-western part of map sheet M-35-XXII. Deposition of this sequence offsets the basement block subsidence and sea basin occupies the fore-slope portions of Podilskiy uplift of Ukrainian Shield. In Early Babynskiy time aleuro-pelite tuffites were depositing. Structure-texture rock features suggest for their development under coastal shallow-water conditions, actually without coarse-clastic material input indicating stable tectonic environments. The rock boundary strike is south-western and is extended outward the fields adjacent from the west. Apparently it is caused by the block uplift provided the barrier for the rocks distribution further to the south-east. The southern part of the area (Pivdennobuzka LTZ) over that time kept higher hypsometric position and had been not covered by sea. The long-term elevated position and tectonic breaking facilitate weathering processes and basement rock destruction with erosion-tectonic relief forms development. In Late Babynskiy time

109 (Bakhtynskiy) the sea basin covered entire western part of the area. The fault-block activation upgrades erosion basis, active weathering crust erosion and removal of essential amount of clastic material to the basin, first of all from the south-east. In the north of the territory (Khomorska LTZ) the pyroclastic rocks including tuffs and tuffites are deposited. In the middle map sheet part, at the modern area between Sluch and Buzhok rivers, volcanic products had got actively mixed with terrigenous sediments provided the columns composed of transitional rocks – tuff- sandstones, tuff-conglomerates, their volcanomictic varieties. The band of these transitional columns is extended in the south-western direction making distinct rim around possible tectonic termination. In the south of map sheet (Pivdennobuzka LTZ) the deeply eroded crystalline basement is overlain by weakly-sorted coarse-clastic Bakhtynski layers. They fill up depressions, valley-like dimples in the relief, which apparently are related to the zones of tectonic breaks. The modern valley of South Bog river corresponds to one of these depressions. Thickness of sediments varies in the wide range and lithotypes are variable. By the fragment composition of their basal portions the link is observed with basement rock developed in the given area. In Late Volynskiy time sea basin ingression continued to the south-east. Simultaneously, in the west (map sheet M-35-XXI) the basalt flows occurred which separated the eastern basin part from the open sea. Over there, the sandy-clayey Slutska Suite and Vinkovetski layers were depositing under steady stagnant conditions, combined in the single sequence. In Khomorska LTZ, however, this sequence column is more differentiated because of differences in bedrock composition. At the end of Volynskiy time tectonic re-arrangement in the area is completed and sedimentation basins are changed. Late volcanism in VPT is controlled by the north-west-trending faults, cross-cutting to previous Riphean and Early Vendian breaks. Odesko-Kovelskiy trough is developed along the south-western EEP margin where sea basins of VPT and Prychornomorya are combined and Mogyliv-Podilska Series is deposited. At the boundary of Early and Late Vendian climatic conditions are changed from arid to warm and wet. This apparently had caused development of more mature (kaolinite) weathering crusts. Erosion products of the latter in Olchedaivskiy time were transported by permanent and temporary water flows into the coastal area of sea basin where feldspar-quartz diverse-grained sandstones with significant kaolinite content were depositing. Waters turbidity precludes activity of organisms. In Lomozivskiy time sedimentation is stable and rhythmic. Conditions were created for spineless fauna and micro-phyto remnants appearance in Podilskiy uplift of Ukrainian Shield. In Yampilskiy time sea basin had been further shortened and its coastal line got away from the source regions. In the north-western direction the sediment lithology changes from mainly sandy to clayey ones. In Lyadivskiy time the basin becomes shallow and gets stagnation features and sulfur hydrogen enriched, mud sediments predominate. The trend of basin shrinkage is kept in Bernashivskiy and Bronnytskiy times. In the latter period volcanic ash from Dobrudja was introduced into the basin [28].

36Mesozoic and Cenozoic stages

Upon the long time of relative tectonic stability with elevated land, weathering crust development and prevailing denudation, Kimmerian activization had caused minor subsidence of the western part in Cenomanian time. From the west the sea had transgressed where shallow-water sediments were depositing with characteristic for these paleo-basin conditions glauconite-quartz sandstones with flint nodules (Pylypchanska Suite). Subsidence area was inherited and encompassed just the western slope of Ukrainian Shield. The basin had existed over Turonian time when Ozarynetska Suite was depositing, which, like Pylypchanska Suite, is developed on the Shield slope. Ozarynetska Suite boundary is sub-parallel to the boundary of Pylypchanska Suite. Ever since this time and until beginning of Middle Eocene most part of the area was the land where weathering and denudation processes continued. The general territory uplift at the beginning of Alpine tectogenesis had been accompanied by some changes in tectonics of the area, specifically, the differences in development of its south-western and north- eastern parts emerged providing the ground for Khmelnytska and Berdychivska LTZs definition respectively. In Berdychivska LTZ the continental regime was kept in Paleogene. Eocene stage over there is expressed in Buchatska Series composed of alluvial sands of the river course and flood-land facies. The rocks distribution is controlled by paleo-valleys of erosion-tectonic origin developed over the surface of weathering crust and related to the fault tectonics activation in Khmilnytska zone. In Kyivskiy time, due to descending motions in the western part of Ukrainian Shield, the channel appeared which connected Paleogene sea basins in the northern and southern parts of Ukraine. In Middle Eocene time this led to the development of Kyivska and Obukhivska suites in Khmelnytska LTZ. The boundary of deeper-water sediments of Kyivska Suite coincides more or less with the eastern boundary of pre-Paleogene

110 sediments. The coastal line of Obukhivske sea was located much further to the east, in places it was curvilinear, often with narrow bays at the depressions of basement relief. At the end of Eocene, because of new cycle of Alpine tectonic activity, the western part of Ukrainian Shield was also involved in uplifting. In Berdychivska LTZ the Early Miocene stage is related to the transgression of Poltavske sea-lake from Dniprovsko-Donetska Depression through the central part of Ukrainian Shield. In this low-salinity basin the rocks of Novopetrivska Suite were depositing. They are developed in the far north-eastern part of Berdychivska LTZ at the small-scale sites preserved from erosion in the dimples of crystalline basement surface. The boundary of Middle and Late Miocene, according to paleo-climatic analysis, is marked by the global cooling and climate aridization. Progressive cooling at the end of Middle Miocene had led to considerable basin shortening and erosion basis descending, resulted in strong erosion activation at the beginning of Late Miocene. That time, at the beginning of Sarmatian time, the ancient mainly sub-longitudinal hydro-network was created. The older sediments, basement rocks and their weathering crusts are being eroded. The branched depression system is developed where continental alluvial sediments were depositing, in places with brown coal interbeds (sequence of coaliferous sands and clays). These are depressions where the Early-Sarmatian sea had transgressed to from the south-west, and in the deepest portions carbonate rocks were depositing. Following existed paleo-valleys, sea bays had entered far to the north providing river damming and deposition of the upper part of the sequence of coaliferous sands and clays. At the end of Early Sarmatian time transgression reached its peak. The favorable climatic conditions facilitated fauna development and limestone sedimentation. At the end of Middle Sarmatian the sea escaped. In Khmelnytska LTZ the territory uplift continued in association with denudation processes and material removal. In Berdychivska LTZ uplift was less extensive and in the residual fragments of Poltavskiy basin, in numerous desalinated lagoons and lakes the clays were depositing. At the sites deliberated from the water, the weathering and oxidation processes had led to the clay parti-coloring. Since the beginning of Pliocene time the steady continental conditions established in the area. In Berdychivska LTZ and eastern part of Khmelnytska LTZ sub-aerial and sub-aqueous sediments of red-brown formation were depositing through weathering of the older rocks. In Khmelnytska LTZ denudation processes predominated. In Eo-Pleistocene and Early Neo-Pleistocene sedimentation was defined by alternating cold and warm phases. During the short cold phases, aeolian-deluvial sediments of Berezanskiy, Illichivskiy, Pryazovskiy and Tyligulskiy climatoliths have been deposited at the elevated sites of watershed plateau, and over the warm phases the soils of Kryzhanivskiy, Shyrokynskiy, Martonoskiy, and Lubenskiy climatoliths were developed. Beginning of Dniprovskiy time is marked with strong cooling and continental glaciation. Along the glacier margin the lakes appeared which periodically went trough the river valleys. Glacier water flows had filled existed river valleys of South Boug, Buzhok, expanding their boundaries. In the north of map sheet the older rocks were eroding and instead of these alluvial-fluvio-glacial, as well as lake sediments were depositing, and in the southern part transitional valleys were developed – Khmilnytsko-Lukashivska and Letychivska. At the watersheds and their slopes the loess-like loams, in places thick enough, were depositing over Dniprovskiy time. In the second half of Middle Neo-Pleistocene and over almost entire Late Neo-Pleistocene the soil- forming processes of warm phases predominated, except Buzkiy time when thick aeolian-deluvial sediments were developed. At the end of Late Neo-Pleistocene time the relief was formed which actually corresponds to the modern one. The well-developed network of active gullies and ravines as well as anthropogenic relief forms indicates that the relief development continues nowadays.

111

87. GEOMORPHOLOGY AND RELIEF-FORMING PROCESSES

According to the scheme of geomorphologic zonation [6], the map sheet area is located within three regions: 1 – Khmelnytska structure-denudation medium-cut height (III-3-48) (constituent part of sub-region of Podilska structure-denudation height over Neogene and Cretaceous sediments (III-3), and this, in turn, of Volyno-Podilska region of sheet-denudation heights – III); 2 – Lyubarsko-Chudnivska accumulative-denudation, alluvial-water-glacial low-cut height (IV-2-59); 3 – Starokostyantynivska denudation high-cut height (IV-2-60). Two latter regions comprise the constituent parts of the sub-region of West-Prydniprovska sheet-denudation height over Precambrian rocks (IV-2), and, respectively, Prydniprovsko-Pryazovska region of sheet-denudation socle heights and lowlands – IV. In tectonic respect, geomorphologic sub-regions include respectively West- Prydniprovska and Podilska II-order morpho-structure. Their conventional boundary coincides with the boundary of Vendian sediments (beginning of the slope of Ukrainian Shield). In the western map sheet part, in Podilska morpho-structure, the basement surface plunges down and hypsometric level of modern surface becomes higher indicating relief inversion. Sedimentary cover consists of Verdian terrigenous sediments, Upper Cretaceous and Eocene marine sediments, Upper Miocene continental and marine rocks, and Quaternary continental sediments. Most part of the territory is located in West-Prydniprovska morpho-structure. The crystalline rock surface is overlain by Eocene marine and partially continental sediments, Upper Miocene and Quaternary continental and marine sediments. Depending on the influence of erosion-accumulative activity of melted waters from Dniprovskiy glacier on the relief development, the territory is divided in two zones (after B.D.Vozgryn – sub-regions [19]): the Northern peri-glacial and Central-Ukrainian. Based on obtained geological data, satellite image processing results, morpho-structure analysis (S.Yu.Bortnyk and others), by the sedimentation conditions, hypsometric position, sediments erosion mode and thickness of preserved sediments, in the studied territory the authors have distinguished 9 structure-geomorphologic sub-areas. In the Northern peri-glacial zone these include Lyubarska alluvial-water-glacial low-cut plain (IV-2-59-a), Sluch-Khomorska (IV-2-60-a) and Ikopotska (III-3-48-a) accumulative-denudation medium-cut plains, Sluch-Teterivska accumulative-denudation low-cut plain (IV-2-60- b), Khmilnytsko-Lukashivska transitional valley (IV-2-60-c); in the Central-Ukrainian – Litynska (IV-2-60-d), Trebukhivska (IV-2-60-e), and Khmelnytska (III-3-48-b) elevated denudation high-cut plains, and Letychivska transitional valley (IV-2-60-f).

37Northern peri-glacial zone

Lyubarska alluvial-water-glacial low-cut plain is located in the northern and north-eastern parts of map sheet. Altitudes vary from 230 to 270 m, slightly decreasing in the north-eastern direction. In tectonic respect, the area is confined to Berdychivskiy block. Conventional boundary with Sluch-Khomorska and Sluch- Teterivska accumulative-denudation plains is set by the boundary of water-glacial sediments. Major genetic relief types are denudation-accumulative and alluvial. The area morphology is defined by the development of water-glacial sands that soften relief forms, and by close location of basement surface. The plain uniformity is broken by the river valleys, gullies, and small swamped dimples. The gully slopes are low, flat, slightly-wavy, sodded, which are progressively substituted by the low watersheds. The gully bottoms are flat or slightly concave, wetted and in places slightly swamped. Technogenic forms include dumps, dams, ponds, irrigation channels, quarries. Ikopotska accumulative-denudation medium-cut plain is located in the north-west of map sheet. From the north it is limited by Khomora river valley, from the south – Sluch river, the eastern boundary with Sluch- Khomorska accumulative-denudation medium-cut plain coincides with the boundary of Vendian sediments. In tectonic respect, the north-western part is located in Grytsivskiy block, and the south-western – in Veselivskiy block. The blocks are separated by Teterivska tectonic zone. Geology includes Vendian terrigenous rocks, Upper Cretaceous, Eocene and Upper Miocene marine sediments, and Quaternary continental sediments. Altitudes of the loess plateau and its slopes vary in the range 260-344 m with the general inclination from the south to north. Major genetic relief types are accumulative- denudation and alluvial. Plateau is cut by the branched network of rivers and gullies. Gully bottoms are broad, flat, highly swamped. The slopes are flat, concave. The gravity relief forms – ancient slides are observed somewhere on the steep slopes of river and gully valleys.

112 Sluch-Khomorska accumulative-denudation medium-cut plain is located in the central part of the northern half of map sheet. In tectonic respect the most part is located in Starosynyavskiy block. Geology includes Upper Miocene marine (sandy-clayey) and Quaternary sediments. Plateau and its slopes are composed of aeolian-deluvial loess-like loams 5-25 m thick. Altitudes of the loess plateau and its slopes vary in the range 245-329 m with general inclination from the south to north. Plateau is highly cut by the river network – Sluch and Khomora branches and gullies. Major genetic relief types are accumulative-denudation and alluvial. On the steep river valley and gully slopes the gravity relief forms are widely developed, mainly ancient slides with sodded detachment walls. On the plateau and its slopes suffusion-collapse relief forms are developed – saucer- like dimples up to 1.5-2.0 m deep, from 50 to 200 m in diameter. The dimples are high-wetted with meadow plants and are caused by collapsing in the loess-like loams. Sluch-Teterivska accumulative-denudation low-cut plain is located in the north-eastern part of map sheet. Geology includes Eocene (Buchatski) continental sediments developed over crystalline basement rocks in the erosion depressions. Upper Miocene sandy-clayey sediments in the east are overlain by parti-colored and in places red-brown clays. Quaternary sediments include water-glacial and lake-glacial sands, overlain by thin loess-like loams, in places with interbeds of buried soils. Major genetic types of relief are accumulative- denudation and alluvial. Loess plateau is cut by deep gullies of Sluch, Teteriv and South Boug river branches; general plateau inclination is to the north-east. Altitudes vary in the range from 229 to 318 m. Maximum surface altitudes – more than 300 m, are observed at the watershed plain. Direction of some hills and ridges is north- western, parallel to the predominate direction of hydrographic network. River valleys within loess plateau are well-developed, the slopes often are steep and complicated by crystalline rock exposures. The upper course of Teteriv river is located in the area. The river flood-lands are often swamped. At the watersheds suffusion- collapse relief forms are developed – minor “saucers” from 20 m to 0.5 km in size. Khmilnytsko-Lukashivska transitional valley is located to the south from Sluch-Teterivska accumulative-denudation low-cut plain, it is linear in the plane and extended in the south-eastern direction; from the south-west it is bounded by the right bank of Domakha river valley. In geostructure respect the valley is controlled by Khmilnytska tectonic zone. The valley is cut into eroded surface of Upper Miocene sandy-clayey sediments. Occurrence of Eo-Pleistocene – Lower Neo-Pleistocene rock remnants, developed like islands, allows assumption that the valley is related to the older hydro-network established after Sarmatian sea regression. Thick water-glacial sediments of Dniprovskiy climatolith, trough-like cross-profile especially in its right bank, indicate that completely the valley is formed by the melted waters of Dniprovskiy glacier. Major genetic type of the valley relief is alluvial with superimposed sub-serial forms. The surface is smoothed, slightly-wavy. The surface altitudes are 280-310 m. The rivers that inherit transitional valley are oriented in the north-western and south- eastern directions and flow in different directions. In the flood-lands of Domakha and South Boug rivers the lowland peat swamps are widely developed. In Khmilnytsko-Lukashivska valley three buried valleys of melted glacier water discharge are distinguished [28]. One of these (northern) spatially coincides with the modern valley of Fosa river, its width is up to 2.5 km in the middle course, and length – as much as 23 km. The second ancient valley is noted along Pishchanka river valley (left branch of South Boug) up to its upper course and then through the linear section is traced in the north-western direction into the valley of unnamed branch of Pozharka river (nearby Shpychyntsi village). In the south-east the valley adjoins South Boug river. The valley width is from 1.3 km in the south-east to 3 km in the north-west, the length is about 15 km. The third valley follows the line of Sokolova-Kumanivtsi- Shpychyntsi villages. The south-eastern part is inherited by the left branch of South Boug river. In the north-west paleo-valley is expressed in the dry trough-like and swamped at the mouth valley inclined to the north-west. Further to the west its direction coincides with the direction of Pozharka river. The valley width is from 1 to 1.7 km, it is traced over the distance of 15 km. Two latter buried valleys adjoin South Boug river which inherits at the given site the ancient hydro-network.

38Central-Ukrainian loess zone

Litynska elevated denudation high-cut loess plain is located in the southern part of map sheet and in extended from the north-west to south-east with gentle inclination in the east-south-eastern directions. Modern relief altitudes vary in the range 300-365 m in the west and 280-340 m in the east. This is the major watershed of South Boug and Sluch rivers with subordinate watersheds of Buzhok, Ikva and Domakha rivers. In tectonic respect Litynska plain is located in Medzhybizkiy and Starosynyavskiy blocks. Geology of Litynska plain includes Upper Miocene limestones and sandy-clayey sediments, Upper Miocene – Pliocene parti-colored and red-brown clays, and Quaternary sediments. Prevailing genetic relief types include denudation at watersheds and accumulative-denudation on the slopes. Alluvial type is also widely developed in the river valleys and gully bottoms. The dense, tree-like gully

113 network is developed in the area with numerous bifurcations up to 10 km long. In the upper courses they are mainly V-shaped with low cut and gradual transitions into the convex watersheds. Toward the mouth the gullies become U-shaped, rarely trough-like with symmetric, sodded, mainly slightly-concave slopes. Cutting depth increases up to 10-25 m and bottom width attains first tens of meters, in places up to 100-150 m. Deep gullies are cut into the water-bearing horizons and permanent water-streams appear in their bottoms. The gorges are developed on the steep slopes where loess sediments are observed at the surface. Gorge length is from some meters to first tens of meters. Cutting depth (from 1.0-1.5 to 5-7 m) depends on the loess thickness. Gravity relief forms are confined to the steep gully slopes. The ancient slides predominate with sodded detachment walls and variously eroded bodies. Denudation relief forms are developed in the South Boug river valley in the single crystalline basement rock exposures. Trebukhivska elevated denudation high-cut plain is located in the south of map sheet. From the north it is bounded by the right bank of South Boug river valley, in the west it adjoins Khmelnytska elevated denudation high-cut plain, and in the east adjoins Biletske uplift. Basement altitudes are mainly high (260-290 m) and Quaternary sediment cover is thin (5-15 m). Surface altitudes are 280-360 m. The plain is located in Medzhybizkiy block and Letychivska tectonic zone. Major genetic relief type is accumulative-denudation with some predomination of denudation processes, variously expressed at different sites due to differentiated tectonic movements in the area. Over most part of the sub-area Upper Miocene rocks are overlain by Upper Neo- Pleistocene sediments only, in the area of Lysogirka village – very thin. In the eastern part, directly below Holocene soil, the rocks of Zavadivskiy climatolith are observed, which, in turn, overlie Lower Neo-Pleistocene sediments. The given site is well expressed in the satellite images by minor dome uplift. In the western part of Trebukhivska elevated denudation plain the loess rocks of Dniprovskiy climatolith lie directly above Upper Miocene sediments. The data presented indicate steady general uplifting in the area starting from post-Miocene time. The gorge-gully network with numerous extensions is tree-shaped. Its structure and cutting depth are identical to those described in Litynska elevated denudation plain and differ in lesser gully density and length. Steep slopes are also often complicated by minor slides. Young slides located nearby Grushkivtsi village, exhibit well-expressed detachment walls up to first meters high and hilly body surface. Denudation remnants are mainly developed along the Vovk river valley which transects Trebukhivska elevated plain from the south-west to north-east. On the steep slopes minor limestone exposures are observed therein. Khmelnytska elevated denudation high-cut plain is located in the south-western part of the studied territory. It is bounded from the north by Sluch river valley and from the east its conventional boundary coincides with the boundary of Vendian sediments. In geostructure respect the plain corresponds to the beginning of the western slope of Ukrainian Shield. The relief development in the area had occurred under conditions of extensive uplifting facilitated reverse relief formation. Neo-tectonic structure plane of the territory is not conformable to that of crystalline basement. Geology includes Vendian terrigenous sediments, Upper Cretaceous and Eocene marine rocks, Upper Miocene continental and marine sediments, and Quaternary continental sediments. Hypsometric level of the modern surface is the highest in the studied territory and at the watershed of South Boug – Buzhok rivers is up to 395 m, South Boug – Vovk – up to 384 m, Buzhok – Sluch – up to 377 m. The relief of Khmelnytska elevated denudation plain in genetic respect belongs to denudation and accumulative-denudation. Denudation processes predominate. The Neogene rocks, elevated to considerable altitudes, are overlain by thin (up to 5-7 m) Upper Neo-Pleistocene sediments. Differentiation of tectonic motions is resulted in the thinnest Quaternary sediments developed in the south of the territory at the watershed of Vovk and South Boug rivers. The watershed plateau-like sites are cut by the valley-gully network. The gullies are narrow in the upper courses with relatively steep slopes, often with minor gorges. In the middle and lower portions the gully bottoms are mainly broad and swamped. The slopes are flattened, sodded, and gradually substituted by the bottoms. On the steep gully slopes the gravity relief forms – slides are developed. Technogenic relief forms include quarries, peat operations, ponds, dams, irrigation channels, railroad heaps and hollows, cleaning facilities. Letychivska transitional valley is located in the south-eastern part of map sheet and extended in the south-eastern direction. Maximum width in the middle part is up to 15 km. The surface altitudes vary in the range 270-310 m with some inclination in the eastern and south-eastern direction. In the south-west it adjoins Biletske uplift where relief altitudes are 300-315 m. Development of the valley is related to the melted waters of Dniprovskiy glacier although it is probably even older. It is evidenced by the occurrence of small-scale sites composed of alluvial sediments of Budatskiy ledge, which are overlain by Martonoskiy-Zavadivskiy climatoliths preserved from erosion. In general, the distinct features of Letychivska valley include significant denudation of

114 Upper Miocene sediments, lack of the sequence of parti-colored clays, Pliocene and Eo-Pleistocene sediments, and development of thick (up to 20-30 m) alluvial-fluvil-glacial and lake sediments. Many authors consider Letychivska valley as the terrace composed of ancient alluvial sediments of South Boug river which formerly flowed in the directions Letychiv – Lityn and further to Vinnytsya. It is not excluded that its development is related to the older river network or ancient Upper Miocenen – Pliocene transitional valley whose sediments were eroded. From the north and south the valley is bounded by the watershed heights. In the western map sheet part its boundaries coincides with the back sutures of the fifth-sixth terraces of South Boug and Buzhok rivers. To the east from Letychiv town it is expressed in the relief by the terrace-like bench in the section Bokhny – Litynka villages. Genetic relief type in the valley is denudation-accumulative with superimposed sub-aerial forms, as well as swamped depressions and suffusion-collapse “saucers”. The valley relief is slightly-wavy, weakly-cut by gully network. The gullies are mainly short (up to first kilometers), low-branched, with low cutting and flattened sodded slopes. In the area of Kopachivka village and to the south-east from Letychiv town the break-trough sites are observed, extended in the south-eastern direction, from first hundreds of meters to 1.5 km wide, actually linear, U-shaped, with flattened slopes and reverse-oriented water flows, separated by weakly expressed watersheds. Fluvial relief forms in the map sheet area include the valleys of South Boug and Sluch rivers, with their flood-lands and over-flood terraces, as well as gullies.

74Sluch river valley

The biggest river in the northern map sheet half is Sluch with branches Khomora and Derevychka. In the west Sluch flows on the slope of Ukrainian Shield where Vendian, Mesozoic and Cenozoic rocks are developed. Further on from Starokostyantyniv town it flows on Ukrainian Shield. By the valley morphology in the map sheet three sections are distinguished which are well expressed in the long-wise river profile. In the first section the valley is expanded, lake-like (from Starokostyantyniv town to Kalynivka village), with asymmetric slopes. Over-flood terraces are developed on the right flat and low bank whereas left bank is steep and high. The high- and low-level flood-lands are distinguished over there, two over- flood terraces and the fragment of third over-flood terraces. In the second section (from Kalynivka village to Korzhivka village) the valley is narrow, canyon-like. The cut into crystalline rocks had created distinct valley relief with cliffy slopes. In the third section the valley is expanded with relatively low banks caused by development of Miocene sandy-clayey sediments and Middle Neo-Pleistocene water-glacial sands. Over-flood terraces are developed in both banks and gradual transitions are somewhere observed in between. Flood-land terrace in the section Starokostyantyniv town – Ostropil village is narrow, some tens of meters wide, rarely 100-200 m. Flood-land is partially swamped with dense swamp vegetation, composed of sandy-clayey material, in places modern sediments consist of peat. The low-level, 0.5-1.5 m high, and high-level up to 2-3 m high flood-lands are distinguished. The high-level flood-land is observed nearby Gubyn, Kalynivka and Ostropil villages. Down the stream from Ostropil village, before merging with Popivka river, the flood-land is 200-350 m wide and up to 2-3 m high above river course; nearby Lyubar town it is expanded up to 1 km. The first-second (Vilshansko-Desnyanska) over-flood terrace is widest up to 3 km at the merging point with Taranka river nearby Koran village. From Starokostyantyniv town to Gubyn village terrace is discontinuously developed in the right bank. Terrace width is 400-2000 m, height is from 1-2 m above flood- land to 6-7 m above river course in the back part, type is erosion-accumulative. From Gubyn village to Pedynka village terrace is absent. It appears again in the right bank nearby Pedynka village and is observed up to Noviy Lyubar village. From Gromada village to the northern map sheet border it is first developed in the left bank and then in the both banks. Width is up to 1000 m, height – up to 2 m above flood-land, in the back part up to 6-8 m above river course; type is accumulative. Terrace sediments up to 13 m thick include loams, rarely sands and sandy loams. The third-fourth (Cherkasko-Trubizka) over-flood terrace of erosion-accumulative type is developed in the right bank from Starokostyantyniv town to Gubyn village. Width is 1000-4000 m, narrower at Kalynivka village. Height is from 8 to 12-16 m above river course in the back part. From Korzhivka village to Vygnanka village terrace is one-sided, right-bank; down the stream it is developed in both banks. Its width increases from 1000 to 3000 m; type is accumulative. From Pedynka village to Gromada village, where the first terrace is absent, the second one directly adjoins the flood-land and is up to 3000 m wide. Terrace surface is flat, inclined towards the river course. The fragment of fifth-sixth (Krukenytsko-Khadzhybeyska) terrace is distinguished after the surface with altitude 290.0 m and bench in the relief. It is observed in the right bank nearby Grygorivka village. Terrace is sculptured. It was developed under relative territory uplift. Alluvial sediments are absent.

115

75South Boug river valley

In the map sheet southern part South Boug river with numerous branches creates the complex branched river network. The major river flow direction is east-south-eastern. The biggest branches in the map sheet include Buzhok, Vovk, Ikva rivers. South Boug river valley morphology essentially differs at various sections and is mainly caused by geology of the territory. In the first section the valley is wide, deep, trough-like. The elbow-like turns reflect block structure of crystalline basement. In the section Novokostyantyniv – Guli villages, where river cuts crystalline rocks, the rapids and cliff exposures are observed in the river course while the cut into the basement rocks is 15-20 m deep. In the third section the river follows direction of Khmilnytsko-Lukashivska transitional valley with broad swamped flood-land and two terraces. In the valley, at various sections, the flood-land and up to three over-flood terraces are distinguished. Flood-land. The flood-land width varies considerably. The greater – up to 1.0-3.0 km is observed in the slope of Ukrainian Shield, from the western map sheet border to Goloskiv village and also in places of South Boug merging with its Buzhok and Vovk branches. In the western map sheet part the flood-land with peat bodies is dried by irrigation channels. Nearby Letychiv town significant part of the flood-land is occupied by water reservoir. The flood-land is absent in the section Novokostyantyniv-Guli villages. The first-second (Vilshansko-Desnyanska) over-flood terrace is erosion-accumulative and discontinuously developed along both banks of South Boug river in the narrow bands up to 300 m wide, 1-2 m high above flood-land, and 5-7 m in the back part. In the western map sheet part it is probably modified in the course of irrigation works. From Stavnytsya village to Shchedrova village terrace is expressed in the relief almost throughout along the left bank. Apparently part of terrace is flooded by water reservoir. In the section from Stavnytsya village to the merging of South Boug and Ikva along the right bank it is actually absent except the minor fragment to the north from Letychiv town. The third-fourth (Cherkasko-Trubizka) over-flood terrace is best expressed in the relief, with clear back suture, from 5-7 m to 10-15 m high in the back part. Along the right bank it is absent at the sites Golovchyntsi village – Letychiv town and Novokostyantyniv-Guli villages, and in the left bank – from the western map sheet border to Chervona Zirka village, between Rusanivka village – Medzhybizh town, as well as in the area of Kopytyntsi village and from the southern outskirt of Kudynka village to the merging of South Boug and Ikva rivers. Terrace is sculptured. Its width is 0.6-1.0 km, maximum (nearby Letychiv town) – up to 2.2 km. Terrace surface is normally flat, with slight inclination towards the river course. Lack of alluvial sediments in many places indicates that its development occurred under general territory uplifting and erosion basis descending. Fifth-sixth (Krukenytsko-Khadzhybeyska) over-flood terrace is most clearly expressed in the relief along the right bank from the western map sheet border to Golovchyntsi village and along left bank from Stavnytsya village to Shchedrova village and in the area of Kopytyntsi village where its small fragment is observed. In some places (Pyrogivtsi village – Medzhybizh town and Golovchyntsi village – Letychiv town) it is overlain by thick sediments of Kaydatsko-Prychornomorskiy climatoliths and in the modern relief it lost terrace morphological features. Terrace maximum height is also noted therein – 20-25 m above the water line. From Letychiv town to Novokostyantyniv village its back suture is expressed in the relief discontinuously apparently due to erosion activity of the melted waters of Dniprovskiy glacier. Terrace is sculptured; it was developed under relative territory uplifting with predominated side erosion in places where the socle is composed of limestones. Terrace is widest – 5.5-5.8 m to the east from the northern outskirt of Letychiv town. Denudation relief forms are mainly composed of limestones, rarely the rocks of crystalline basement. The biggest one, about 9 km2 in size, is composed of reefogenic pearlwort limestones and observed to the north from Letychiv town. Lesser denudation forms are noted in the area of Stavnytsya and Antonivka villages. Buzhok river valley. In the map sheet area this valley is about 40 km long, direction is east-south- eastern. Flood-land is broad – 1.5-2.0 km, swamped actually over entire length. Buzhotske peat deposit is located therein. In the mouth part the flood-land width drops to 50-300 m. In the lower course of Buzhok river three over-flood terraces are well expressed in both banks – the first-second (Vilshansko-Desnyanska), third-fourth (Cherkasko-Trubizka), and fifth-sixth (Krukenytsko- Khadzhybeyska), with slightly inclined surfaces. At the surface of the third-fourth over-flood terrace two small denudation remnants composed of limestones are observed to the north-west from Stavnytsya village. Vovk river valley. The valley fragment of Vovk river is located in the west of map sheet and its mouth part – to the south from Letychiv town. Over entire length of 100-150 m wide flood-land it is swamped, with

116 peat body (Vovkivske deposit). In the mouth part the flood-land is expanded up to 1 km. Minor denudation remnants composed of limestones are observed by both banks and in the are of Revukha village only the rocks of crystalline basement are exposed in the flood-land left bank. Along both banks in the lower course the third-fourth (Cherkasko-Trubizka) over-flood terrace is well expressed. The minor fragment of the first-second over-flood terrace less than 100 m wide is only observed at the southern outskirt of Revukha village. The highest fifth-sixth over-flood terrace is observed in the fragments to the south and north from Revukha village along the right bank of Vovk river. Ikva river valley. The valley commences at the watershed of Sluch – South Boug rivers and flows in the east-south-eastern direction to Mykolaivka village, then it turns up and in the lower course is extended in the south-eastern direction. The river flood-land is up to 1.0 km wide, swamped, with biogenic relief forms. After Mykolaivka village the flood-land collapses to 150-250 m expanding up to 0.7-1.0 km only in places of merging with major branches. The course is narrow (from first meters to 10-15 m), slightly-wavy, with calm flowing. In the lower course the first-second (Vilshansko-Desnyanska), third-fourth (Cherkasko-Trubizka), and fifth-sixth (Krukenytsko-Khadzhybeyska) over-flood terraces are well enough expressed by both valley banks. In the mouth part, however, the geomorphologic contours of fifth-sixth and partly third-fourth over-flood terraces are not clearly expressed. Gorge-gully network. Development of gorge-gully network depends on the local geology, rock lithology and bedding, distance to the surface, tectonic and hydrogeological conditions. In the northern part of the territory (Lyubarska alluvial-water-glacial low-cut plain) the gullies differ in flattened, sodded low slopes which are gradually substituted by the low watersheds, with slightly concave bottoms, often swamped, wetted. The common features are displayed by the gullies in Letychivska and Khmilnytsko-Lukashivska transitional valleys. They are low-branched, with shallow cut, mainly short (up to first kilometers). The loess plateaus located in the northern part of the area are complicated by the dense gully network. The gullies belong to Sluch, Khomora, Teteriv rivers. The slopes are gradually substituted by the plateau. In the loess plateau-like plains of the southern part the dense, tree-like, branched gully network is developed. The gully length attains 10 and more kilometers. In the upper courses they are narrow, with low cut, relatively steep slopes, mainly V-shaped, and with gradual transitions into slightly-convex watersheds. In the middle and mouth parts the gullies are U-shaped, rarely trough-like. Gravity relief forms are mainly developed in the southern part of the territory and in Sluch-Teterivska plain where they are confined to the steep gully slopes. The ancient slides predominate with smoothed and sodded detachment walls up to 3-4 m high and variously eroded bodies. The young slides with well-expressed detachment walls are noted in the area of Grushkivtsi village. By morphology the slides are divided into circus- like and frontal. Suffosion-collapse relief forms. The steppe saucers are developed on the slopes of Sluch-Teterivska and Sluch-Khomorska accumulative-denudation plains, at the surface of Letychivska and Khmilnytsko-Lukashivska transitional valleys. These are closed flat-bottom dimples, normally oval or rounded, 50.0-200.0 m in diameter in average, 1.5-2.0 m deep, rarely up to 2.5-3.0 m. The saucer bottoms are slightly concave, mudded, weakly draining water at the spring snow melting and rain times, resulting in their periodical swamping. Development of these relief forms is facilitated by the occurrence of loess-like loams and low-cut local relief. Technogenic relief forms. In the map sheet area these include: water reservoir (South Boug river); numerous ponds of which the biggest ones are located in the Buzhok, Vovk, Ikva river valleys; quarries; clay ponds; dams; road heaps; peat operations; drainage trenches, sugar plant tailing in the areas of Khmelnytskiy town, Starokostyantyniv town, Stara Synyava and Ivanopil villages.

117

98. HYDROGEOLOGY

According to the scheme of zonation of Ukraine with regard to the groundwater development, the western part of map sheet M-35-XXII is located in Volyno-Podilskiy artesian basin whereas remaining territory is confined to the western part of Ukrainian basin of fractured waters (Fig. 8.1). In the Ukrainian basin of fractured waters the depth of crystalline rocks and contained groundwaters is low. The water-bearing horizons in Paleogene, Neogene and Quaternary sedimentary sequences in the solid blanket cover crystalline basement and are only lacking somewhere on the river valley slopes.

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II-III f,lgP Z aH Ns M II 1 Z-K 8.6 3.0 N!s MZ Z n.a. -KZ 1-6 aH 4.0 0.6 GRYTSIV vd,ePIII 1-6 254.8 aP aH 1-6 II-III aP II - II I aPII-III f,lgP II 1-6 f,lgP M 6 976 AR–PR AR–PR1 II 1 Z fP II -K M aP Z Z-KZ II-III 9AR–PR 19.7 1 121.0 n.a. 795.0 7.97 M Z- 139 95.0 21.0 0.7 KZ 16.8 Ns n.a. 10.0 260.0 233.7 0.8 1 44.0 0.8 290.0 1 LYUBAR f,lgP II AR–PR 3.8 1 3.1

f,lgP N II !ò ç 1-6 AR–PR Ns 13 1 1 aP 16 Ns II-III 129 1 15AR–PR n.a. 7.6 146.9 37.0 1 11.8 n.a. MZ-KZ 95.0 0.3 1.0 0.6 n.a. 11.4 260.0 310.0 MZ-KZ 14.6 0.4

M 280.0 Z - K N Z !ò vd,eP Ns ç III Ns 1 1 Ns N!s 1-6 1 aP 23 AR–PR1 II-III Ns 24 1 155.5 24.0Z Ns n.a. MZ-K 172.8 28.0 1 11.0 0.5 n.a. AR–PR 78 1 1-6 5.0 0.4 280.0 M

Z 120.0

300.0 K s Z ! aP AR–PR n.a. N 11.0 II-III 1 AR–PR 30.0 0.8 1

AR–PR Z 28 1 266.0 K - Z AR–PR1 69.1 21.0 M 1Vvl n.a. 1 Ns 17.0 0.8 2 1 81AR–PR 1.379 4.8 Ns1 290.0 Ns 1 5.2 aH 1 1.5 1-6 216.0 MZ f,lgP-K 0.7 4.8 ÑÒÀÐÎÊÎÑÒßÍÒÈÍ²Â 10.1 II Fe n.a. Z 0.7 5.2) aP 37.0 II-III 0.7 1-6 AR–PR Z 285.0 Ns 1 -K 32 1 Z aP M Ns II - II I 146.9 1 Ns n.a. 23.0 39 1 6.0 0.7 34AR–PR Vvl 1 3 1 300.0 864.0 0.8 16.0 146.9n.a. Ns 1.208 1 Z Z 10.0 Z-K K M - Z Ns 5.0 0.5 M 1 0.6 300.0 Fe 10.0 Ns 1 AR–PR Ï 111 1 @ 85 Ns1 37AR–PR1 èÝ Ns M 1 19.0 Z 69.1 60.5 28.5 - K n.a. n.a. 144.0 Z M 2.0 n.a. 0.6 Z-KZ 1.0 44.0 0.5 14.0 263.0 0.5 310.0 Ns1 AR–PR 291.0 60.5 39 89 1 n.a. 13.5 86.0 39.0 0.7 n.a.

0.7 Z

3.0K 0.7 - Ns

293.4 1

Z vd,eP M II I f,lgP 320.0 II

aH Ns+AR–PR 6 11 432.0 MZ Ns 0.284 -KZ 1 vd,ePIII 8.0 0.6 afPII Ns 4 afPII 1 0.3 3.0 afP 93 AR–PR1 Ns II Ns 1 2.7 120.0 15.0 Ns 1 0.3 n.a. 1 M STARA SYNYAVA 883AR–PR 1 1.0 Z 30.0 - AR–PR 320.0 K 1 143.5 7.4 Z Z -K n.a. Z vd,eP MafP II I 21.6 283.4 0.7KHMILNYK II 94 Vvl1 AR–PR 1 11AR–PR 1 192.4 35.0 1-6 n.a. 129.6 0.996 AR–PR

13.0 N!s Rn 1 22.0 0.9 l 8AR–PR

2 E aPII-III 1 310.0 v 0.7 Kpl+oz+ 13.0 1 0.387

2 V 5.435 Ns -KZ 117.5 0.446 +AR-PR 53 1 Z Rn 1 86.4 61.0 M 0.8 0.340 4.315 n.a. 9 AR–PR 0.4 MZ 1 aH 3.0 -KZ vd,ePII I 102.7 340.0 AR–PR 10 1 vd,eP 55Vvl1 0.7 II I Ns 0.721 81.51.610 86.4 n.a. 26.2 1 Rn Rn D 0.390 0.6 1.315 0.5 -KZ 1.1 Ns MZ -KZ 300.0 56 1 vd,eP Fe MZ 57AR–PR II I 121.0 10.0 1 58 P ob n.a. 64.8 2 15.0 0.5 39.6 Ns 121.0 79.0 Ns 280.0 Ns n.a. 1 n.a. 1 1 21.7 0.7 afP 25.0 0.6 310.0 II 1-6 360.0 aH 1-6 vd,eP aP III II-III

aP N

II-III

Ï Ï

! @

@ s AR–PR ë 59 1 AR–PR 1

61 Ns1 MEDZHYBIZH ë þ þ KZ 43.2 MZ- Ns 7 0.644 121.0 56.0 1 Ns n.a. 47.0 n.a. 1 4 Vmp2 1-6 0.4 5.0 71.0 1-6 0.6 0.5 Z 1.302 13.2 320.0 330.0 aP -K II-III Z MaPII-III 0.8 13.2 1-6 M Ns Z-K N 6Vmp vd,ePIII 1 Z !s 2 aP aH 9.2 3 II-III 3.445 1-6 Vmp 7.8 9.2 2 aH 0.7 _ AR–PR aPII-III Fe 67 1 Ns 1 V 216.0 LETYCHIV @ 10.0 vd,eP n.a. 17AR–PR III ü 1 ç aH 0.2 0.6 178.0 vd,eP 107 V1 vl 295.0 N 75 0.2 II I

!çâ 41.0 0.6 15.0 M

112.0 vd,ePIII M AR–PR

271.7 5Ns 68 1

Z 1

n.a. Z -KZ

- aH

60.0 0.6 K 909.0

Z 1.7 288.0 399 Z 77.8 35.8-KZ

Ns N 9.15 -K n.a. 1 !ç Z 0.5 M

vd,eP â M 4.6 0.4 Ns III 281.5 310.0 vd,eP 1 III

1:500 000 5 kilometers in 1 centimeter

5 0 10 20 25 km

Fig. 8.1. Hydrogeological sketch of map sheet M-35-XXII (Starokostyantyniv).

See next page for the legend.

118

1 1 2 3 12,2 4 5 67

8 91011 1213 14

53 N s 1 86.4 n.a. 61.0 15 16 17 18 19 0.4 20 3.0 159.0 4 3.0 ab10 AR-PR 1 1 AR-PR Ns1 aac 6Vmp2 1 2.7 D 3.445 9.2 81.5 1.610 - 0.644 1 0.7 Rn 21 22 23 24 25 26 9.2 0.6 1.135 0.6 - AR-PR 3.8 bbd E 1 3.1 Fig. 8.1. Continues. The legend.

First from the surface water-bearing horizons and complexes: 1 – water-bearing horizon in Holocene alluvial sediments of river flood-lands and gully bottoms (aH); 2 – water-bearing horizon in Upper Neo- Pleistocene aeolian-deluvial and eluvial-deluvial sediments (vd,ePIII); 3 – water-bearing horizon in Middle- 1-6 Upper Neo-Pleistocene alluvial sediments of the first-sixth over-flood terraces (a PII-III); 4 – water-bearing horizon in Middle Neo-Pleistocene alluvial-fluvio-glacial sediments (afPII); 5 – water-bearing horizon in Middle Neo-Pleistocene water-glacial sediments (fPII); 6 – water-bearing complex in Miocene Sarmatian sediments (N1s); 7 – water-bearing complex in fracturing zone of Precambrian crystalline rocks and their gruss weathering crust (AR-PR1); boundaries of water-bearing horizons and complexes occurring below surface: 8 – water-bearing complex in Sarmatian sediments (N1s); 9 – water-bearing horizon in Miocene Novopetrivska Suite (N1np); 10 – water-bearing horizon in Miocene Podilska Suite (N1pd); 11 – water-bearing horizon in Eocene Obukhivska Suite (P2ob); 12 – water-bearing horizon in Eocene Buchatska Suite (P2bč); 13 – water-bearing complex in Upper Cretaceous Pylypchanska and Ozarynetska suites (K2pl+oz); 14 – water-bearing complex in Upper Vendian Mogyliv-Podilska Series (V2mp); 15 – water-bearing complex in Lower Vendian Volynska Series (V1vl); boundaries of water-proof rocks: 16 – sequence of red-brown clays (N2čb); 17 – parti-colored clays (N1sg); 18 – Eocene Kyivska Suite (P2kv); 19 – weathering crust (MZ-KZ); 20 – water-points (boreholes): above – number in catalogue and geological index of water-bearing horizon; below – borehole altitude, m; to the left in numerator – yield, m3/day, in denominator – water level depression, m; to the right in numerator – water depth, m, in denominator – water mineralization, g/dm3; 21 – water-scoop units operating under approved by State Commission of Ukraine on Mineral Reserves or its territorial bodies exploitation groundwater reserves of a) groundwaters, b) mineral waters: above – number in the list of mineral deposits and occurrences and geological index of water-bearing horizon; to the left: in numerator – bulk yield, th.m3/day, in denominator – 3 3 3 mineralization, g/dm ; to the right: in numerator – reserves, th.m /day, sum of A+B+C1 categories, th.m /d; in denominator – reserves of A+B categories, th.m3/d; to the right – valuable component; 22 – water-scoop units operating under approved by the Scientific-Technical Council of geological enterprises exploitation groundwater reserves: above – number in the list of mineral deposits and occurrences and geological index of water-bearing horizon; to the left: in numerator – bulk yield, th.m3/day, in denominator – mineralization, g/dm3; to the right: in 3 3 numerator – reserves, th.m /day, sum of A+B+C1 categories, th.m /d; in denominator – reserves of A+B categories, th.m3/d; 23 – undeveloped sites with exploitation groundwater reserves approved by a) State Commission of Ukraine on Mineral Reserves or its territorial bodies, b) Scientific-Technical Council of geological enterprises: above – number in the list of mineral deposits and occurrences and geological index of water-bearing horizon; to the left – geological index of water-bearing horizon (complex), in numerator – 3 3 3 reserves, th.m /day, sum of A+B+C1 categories, th.m /d; in denominator – reserves of A+B categories, th.m /d; 24 – water chemical type in water-scoops: a) hydrocarbonate, b) sulphate, c) chloride, d) mixed; 25 – hydrogeological zonation: D – Volyno-Podilskiy artesian basin, E – Ukrainian fracture water basin; 26 – watershed of South Boug and Prypyat river basins.

In Volyno-Podilskiy artesian basin the depth of crystalline rocks and contained groundwaters is great with thick Vendian sedimentary sequence and contained water-bearing horizons monoclinally dipping to the south-west under the angle ~1o, and horizontally-laying Cretaceous, Paleogene, Neogene and Quaternary sediments and related water-bearing horizons.

119 The groundwater feeding and accumulation conditions in the area are favorable enough because of climatic factors and water-bearing rock lithology. General cutting of the modern surface and spatial discontinuity of water-proof rocks facilitate the surface and underground water flow providing extensive water exchange in the draining influence zone of the local river network. According to the geological structure and hydrogeological conditions, the following water-bearing horizons and complexes are distinguished in the map sheet area: 1) water-bearing horizon in Holocene alluvial sediments of river flood-lands and gully bottoms (aH); 2) water-bearing horizon in Upper Neo-Pleistocene aeolian-deluvial and eluvial sediments (vd,ePIII); 3) water-bearing horizon in Middle-Upper Neo-Pleistocene alluvial sediments of the first-sixth over- 1-6 flood terraces (a PII-III); 4) water-bearing horizon in Middle Neo-Pleistocene alluvial-fluvio-glacial sediments (afPII); 5) water-bearing horizon in Middle Neo-Pleistocene water-glacial and lake-glacial sediments (f,lgPII); 6) water-bearing complex in Miocene Sarmatian sediments (N1s); 7) water-bearing horizon in Miocene Novopetrivska Suite (N1np); 8) water-bearing horizon in Miocene Podilska Suite (N1pd); 9) water-bearing horizon in Eocene Obukhivska Suite (P2ob); 10) water-bearing horizon in Eocene Buchatska Suite (P2bč); 11) water-bearing complex in Upper Cretaceous Pylypchanska and Ozarynetska suites (K2pl+oz); 12) water-bearing complex in Upper Vendian Mogyliv-Podilska Series (V2mp); 13) water-bearing complex in Lower Vendian Volynska Series (V1vl); 14) water-bearing complex in fracturing zone of Precambrian crystalline rocks and their gruss weathering crust (AR-PR1). In the studied map sheet the active groundwater interaction is noted and by this reason specific water- bearing horizons are distinguished by stratigraphic principle taking into account the host-rock lithology. Besides the water-bearing rocks, the water-proof sediments are also developed in the sedimentary sequences. Because of discontinuous and limited distribution and somewhere also low thickness, they comprise the local water-proofs. The water-proofs include: - sequence of Pliocene red-brown clays (N2čb); - sequence of Miocene parti-colored clays (N1sg); - Eocene Kyivska Suite (P2kv); - Mesozoic-Cenozoic weathering crust (MZ-KZ). Water-bearing horizon in Holocene alluvial sediments of river flood-lands and gully bottoms (aH) is confined to the flood-lands of Khomora, Ikopot, Sluch, Ikva, Buzhok, South Boug, Vovk rivers and their branches and developed in the narrow bands extended along the river courses. Flood-land width is from 100-200 m to 1.0-1.5 km. Water-bearing rocks include micro- and fine-grained sands, muds, sandy loams and loams laying over Sarmatian sediments; in the valleys of Sluch (down from Starokostyantyniv town) and South Boug (down from Medzhybizh village) – over crystalline rocks; in the north-eastern map sheet part – over fluvio-glacial sediments. Thickness of water-bearing horizon is 1.3-6.1 m, in places up to 10.0 m. Water-bearing horizon is of the ground type. The depth to static levels varies from 0.0 to 6.1 m. The water level altitudes are in the range 264-372 m. Water content of the horizon is low. Daily water yields from wells are 0.2-0.5 m3. The sand filtration coefficients are 0.3-10.0 m/day. Feeding of water-bearing horizon is being performed through infiltration of atmospheric precipitates and water inflow from other water-bearing horizons. Under spring river high water the feeding is being additionally provided from the flood waters. Water-bearing horizon discharge is being done into the river network. The horizon regime is inconstant with seasonal level oscillations 1.0-1.5 m in amplitude. By chemical composition the waters are sulphate-hydrocarbonate calcium, sulphate-hydrocarbonate magnesium-calcium, chloride-hydrocarbonate magnesium-calcium. Because of the local development, low water content and unsuitable sanitary-hygienic conditions the horizon is ineligible for centralized water supplying. Water-bearing horizon in Upper Neo-Pleistocene aeolian-deluvial and eluvial sediments (vd,ePIII) is developed at the watersheds of Ikva, Buzhok, South Boug, Vovk rivers and in the right watershed slope of Sluch river valley in the north-eastern part of the map sheet territory. Water-bearing rocks mainly include loess-like porous loams, sandy loams and sands. At the column bottom thin sand interbeds are observed. Thickness of the water-bearing portion of loams is 1.0-6.0 m.

120 The water-bearing horizon is non-pressurized. The lower water-proof, where given horizon is being formed at the watersheds of Ikva, Buzhok, South Boug, Vovk rivers, comprises Sarmatian clays, and at the watershed of Sluch river – Neogene parti-colored, in places red-brown clays, as well as Sarmatian clays. The water level depth in wells is 0.6-5.5 m. Water level altitudes vary from 248 m to 372 m. Because of low filtration properties of water-bearing rocks, the water content of horizon is low. Daily water yields from wells are 0.2-0.6 m3. Estimated filtration coefficients are 0.05-0.8 m/day for sandy loams and loams and 1-3 m/day for sands. By chemical composition the waters are sulphate-hydrocarbonate calcium and sulphate-hydrocarbonate magnesium-calcium. Feeding of water-bearing horizon is being performed through infiltration of atmospheric precipitates. The feeding regions are confined to the watershed plateau. Discharge is observed in the river valleys and gully bottoms. The horizon regime completely depends on amount of atmospheric precipitates and is susceptible to strong seasonal variations up to 1.2-1.6 m in amplitude. The water-bearing horizon is being widely used by the rural population through shaft wells in the household purposes. Because of low water content it is not suitable for centralized water supplying. Water-bearing horizon in Middle-Upper Neo-Pleistocene alluvial sediments of the first-sixth over-flood 1-6 terraces (a PII-III) is developed along the valleys of Khomora, Sluch, Ikopot, Ikva, Buzhok, South Boug and Vovk rivers. Water-bearing rocks include diverse-grained sands with sandy loam and loam interbeds. Thickness of water-bearing sequence is normally 2-10 m, water column height in wells varies from 0.6 to 3.6 m. The water-bearing sequence is underlain by Middle Neo-Pleistocene water-glacial sediments, Neogene rocks or weathering crust of crystalline rocks. In places water-bearing horizon in alluvial sediments of over-flood terraces is hydraulically connected with underlaying water-bearing horizons. The depth of water-bearing horizon level varies from 2.9-6.0 to 8.1-9.0 m. The water level altitudes vary from 229.5 m (Grynivtsi village) to 286.2 m (Shyborivka village). Water content of horizon is irregular and depends on lithology and granulometric composition of water- bearing rocks. Daily well yields are 0.3-0.6 m3. Borehole yields vary from 0.5 m3/day under depression by 1.0 m (Rosolivtsi village) to 43.0 m3/day under depression by 1.3 m (Masivtsi village). Filtration coefficient of sands varies from 3-5 to 10-15 m/day. By chemical composition the waters are sulphate-hydrocarbonate calcium and sulphate-hydrocarbonate magnesium-calcium. Feeding of water-bearing horizon is being made through infiltration of atmospheric precipitates, in places through inflow from other water-bearing horizons. Discharge is observed in the river valleys. The horizon regime depends on atmospheric precipitates. Because of the local development, irregular water content and contamination the horizon is not suitable for centralized water supplying. Water-bearing horizon in Middle Neo-Pleistocene alluvial-fluvio-glacial sediments (afPII) is developed in the eastern part of map sheet in the Fosa river valley, within ancient transitional valley of South Boug river. Water-bearing rocks include diverse-grained sands and sandy loams of total thickness 2.0-6.0 m and in some places only thickness of water-bearing horizon attains 23.7 m. Water-bearing rocks are mainly developed over Neogene sandy-clayey sequence, partially – over Archean-Proterozoic crystalline rocks and their weathering crust. Water-bearing horizon is non-pressurized. Groundwater level depth is 5.2-10.0 m. Water level altitudes vary from 252 to 290 m. Water content of horizon is low. Daily water yields from wells are 0.3-0.6 m3. Filtration coefficient is 3- 5 m/day. By chemical composition sulphate-hydrocarbonate magnesium-calcium water predominate with mineralization 0.5-1.3 g/dm3. Feeding of water-bearing horizon is being made through infiltration of atmospheric precipitates and inflow from other water-bearing horizons. The horizon is being drained by the modern erosion network. The horizon regime depends on climatic factors, level variation amplitude is 1.0-1.5 m. Water-bearing horizon in Middle Neo-Pleistocene water-glacial and lake-glacial sediments (f,lgPII) is developed in the north-eastern map sheet part in the valleys of Sluch river and its branches. Water-bearing rocks include diverse-grained sands with gravel and pebble, of total thickness 5.0-7.0 m. In places thickness of water- bearing horizon attains 18.6 m. Water-bearing rocks lie mainly over Neogene sandy-clayey sequence and partially – over Archean-Proterozoic crystalline rocks and their weathering crust. Water-bearing horizon is non-pressurized. Groundwater level depth is 3.1-7.3 m. Water level altitudes vary from 239 to 271 m.

121 Water content of horizon is low. Daily water yields from wells are 0.4-0.6 m3. Filtration coefficient is 1- 8 m/day. By chemical composition the waters are mainly sulphate-hydrocarbonate magnesium-calcium and chloride-hydrocarbonate magnesium-calcium. Feeding of water-bearing horizon is being made through infiltration of atmospheric precipitates and inflow from other water-bearing horizons. The horizon is being drained by the modern erosion network. The horizon regime depends on climatic factors, level variation amplitude is 1.0-1.5 m. Water-bearing complex in Miocene Sarmatian sediments (N1s) is the map sheet area is developed throughout except the far north-eastern part. It is also absent in the valleys of Sluch and South Bough rivers with right branches Fosa and Vovk where Sarmatian sediments are eroded. Water-bearing rocks include shell and oolite limestones, quartz sands, diverse-grained, coaliferous, rarely aleurites. The clays, developed in the sequence, except the lower column part, do not provide stable water- proofs because of irregular and discontinuous distribution of clay interbeds both in lateral and vertical directions. In the upper column part the clays comprise relative water-proof facilitating groundwater accumulation in Upper Neo-Pleistocene aeolian-deluvial and eluvial loams. Limestones, developed at the column bottom, are actually completely watered, except drainage zones along river valleys which cut these sediments. Thus, the water-bearing horizons of sands and limestones in Sarmatian sediments are hydraulically connected and, in fact, comprise the common water-bearing complex. Thickness of water-bearing rocks varies from some meters to 31.0 m and is normally 10.0-22.0 m. Sarmatian water-bearing sediments in the western map sheet part (in tectonic respect it is western slope of Ukrainian Shield) are underlain by water-bearing rocks of Eocene Obukhivska Suite, and in the far north-east – by water-bearing sediments of Miocene Novopetrivska Suite and Eocene Buchatski layers. Over remaining territory, within the Shield, Sarmatian water-bearing sediments lie over weathering crust of crystalline rocks. Sarmatian water-bearing complex is non-pressurized in general. The depth, depending on thickness of overlaying rocks, varies from 0.0 to 61.0 m. The depths from 25.0 to 40.0 m predominate. Water level altitudes vary from 243.0 to 323.0 m. Limestone water-bearing sequence in Sarmatian sediments is pressurized. Depending on the drainage rate, the pressure value varies from 1.0 to 23.0 m (DH 14, Rashtivka village, Derevychka river). Water content of the complex varies in the wide range depending on the rock lithology and feeding conditions of water-bearing rocks. Daily water yield from wells in Sarmatian sands vary from 0.3 to 0.8 m3/day. Borehole yields, developed for Sarmatian limestones, are much higher, up to 146 m3/day. Spring yields in the Sluch and Ikopot river valleys, where the waters from this complex are being discharged, are 4.3; 25.9; 34.6; 138.2 m3/day. In Korzhivka village (right slope of Sluch river left branch) the yield attains 216 m3/day. Water conductivity of the complex varies from 102 m2/day to 650 m2/day, piezo-conductivity coefficient – from 1.0×104 to 1.69×106 m2/day. By chemical composition the waters of Sarmatian sediments are mainly sulphate-hydrocarbonate magnesium-calcium, sulphate-hydrocarbonate calcium and chloride-hydrocarbonate calcium. Feeding of water-bearing complex is being made mainly through infiltration of atmospheric precipitates in places of shallow sand and limestone occurrence, and through outflow from underlaying water-bearing horizons. High enough hypsometric position of water-bearing complex facilitates its draining by the river and big gully valleys, expressed in the springs. The level regime is susceptible to the seasonal variations. After longstanding system observation data the level variation amplitude attains 1.0 m. The waters of Sarmatian sediments are being widely enough used by the rural inhabitants with shaft wells and captured springs in household purposes. Normally these are the waters from sequence of sands with near-surface position. The waters in Sarmatian limestone sequence are relatively deeper, high-quality and almost complete lacking or insufficient nitrate content. To date these waters are mainly being used through boreholes for water supplying to rural consumers and centralized water supplying of the towns. After prospecting and exploration the groundwater reserves are identified and approved fro the given horizon for the centralized water supplying of Starokostyantyniv town. Water-bearing horizon in Miocene Novopetrivska Suite (N1np) is only developed in the far north-east of the area in the local sites in the upper course of Sluch river right branches. This water-bearing horizon in the map sheet territory was not studied and its description is given by analogy with adjacent map sheets and also using mapping borehole data.

122 Water-bearing rocks include mainly fine-grained, kaolineous sands with secondary kaoline and kaolineous clay interbeds. Average thickness of water-bearing rocks is 4.0-12.0 m, maximum – up to 16.8 m. The depth of water-bearing horizon varies from 30.0 to 34.0 m, depending on the relief. By the host-rock conditions the waters of this water-bearing horizon are low-pressurized. The maximum pressure value is up to 10.0 m. The horizon is underlain by the weathering crust of Precambrian crystalline rocks and overlain by Sarmatian sediments (clays, sands) and sequence of parti-colored clays. Significant kaoline content of the sands suggest for their low filtration properties and low water content of the horizon. Filtration coefficient varies from 0.4 to 2.0 m/day. Borehole yields do not exceed 58 m3/day, specific yield is 8.6 m3/day. By chemical composition the waters are mainly hydrocarbonate calcium and magnesium-calcium. Water-bearing horizon in Miocene Podilska Suite (N1pd) is developed in the limited area in the southern map sheet part, in the local site on the slopes of Vovk river. This water-bearing horizon in the map sheet area was not studied. The water-bearing rocks include fine-grained clayey sands 5-7 m thick, in places up to 11.0 m. The rocks mainly lie over Archean-Proterozoic crystalline rocks and their weathering crust, and also over Paleogene Obukhivska Suite sediments. The water-bearing horizon is non-pressurized. Groundwater level depth is 45-70 m. Water level altitudes are in the range 255.0-260.0 m. Considerable clay content of the sands indicates their low filtration properties and low water content of the water-bearing horizon. Feeding is being made through water inflow from underlaying water-bearing horizons. The horizon is being discharged outside the studied area into adjacent water-bearing horizons. Because of the low water content, local development and great depth the water-bearing horizon in Podilska Suite sediments is out of practical value and cannot be recommended for centralized water supplying. Water-bearing horizon in Eocene Obukhivska Suite (P2ob) is developed in the western map sheet part, in Volyno-Podilskiy artesian basin. Water-bearing rocks include glauconite-quartz sands and sandstones 6-10 m thick, in places up to 18.2 m. They lie over water-proof sediments of Kyivska Suite, and in places where the latter is absent – over Cretaceous sediments, as well as over basement crystalline rocks and their weathering crust. Water-bearing horizon is pressurized. The pressure value varies from 2.0 to 28.5 m. Groundwater level depth is 16.0-100 m. Level altitudes vary from 265.5 to 281.5 m. Water content of the horizon is low. Filtration coefficient is 1-3 m/day. Borehole yields vary from 95.0 to 144 m3/day. By chemical composition the waters are mainly hydrocarbonate magnesium-calcium and sulphate- hydrocarbonate magnesium-calcium. Feeding is being made through the atmospheric precipitates and water inflow from other water-bearing horizons. The horizon is being discharged into adjacent water-bearing horizons. The waters are being used for the household needs of inhabitants and farms water-supplying. For the centralized water supplying the horizon is out of particular value but can be used together with the water-bearing complex in Sarmatian, Cretaceous and Vendian sediments. Water-bearing horizon in Eocene Buchatska Suite (P2bč) is locally developed in the eastern part of map sheet. Water-bearing rocks include diverse-grained, coaliferous sands on 4.0-20.0 m total thickness, in places up to 25.4 m. Water-bearing rocks lie over Precambrian crystalline rocks and their weathering crust and are overlain by Sarmatian clays and sands. In the map sheet area this water-baring horizon was not studied. The brief description is given based on data from adjacent territories. Water-bearing horizon is low-pressurized, the pressure value is up to 10 m. Borehole yields vary from 8.6 to 86.0 m3/day under level depression by 3-5 m. Groundwater level depth is 10.0-46.0 m. Water level altitudes vary from 240 to 270 m. By chemical composition the waters are mainly hydrocarbonate calcium-magnesium with mineralization 0.4-0.5 mg/dm3. Feeding of the horizon is being made through the atmospheric precipitates and water inflow from other water-bearing horizons. The horizon is being discharged into underlaying water-bearing horizons outside the map sheet area. In the map sheet area the horizon is not being used and not suitable for centralized water supplying because of limited distribution and low water content. Water-bearing complex in Upper Cretaceous Pylypchanska and Ozarynetska suites (K2pl+oz) is developed in the western map sheet part. Water-bearing rocks include sands, quartz-glauconite sandstones, flints.

123 Total thickness is 4.0-16.0 m and in some places only it attains 24.7 m. Water-bearing rocks lie over Upper Vendian Mogyliv-Podilska Series and Lower Vendian Volynska Series and are overlain by Eocene Kyivska Suite sediments. The water-bearing complex is pressurized. Pressure value varies from 7.7 to 24.4 m. Groundwater level depth is 41.8-65.0 m. Water level altitudes are in the range 265-268 m. Water content of the complex is low. The rock filtration coefficients are 1-3 m/day. Borehole yields vary from 26.0 to 190.0 m3/day, specific yields – from 8.6 to 15.7 m3/day. By chemical composition the waters are mainly hydrocarbonate sodium-magnesium-calcium and hydrocarbonate magnesium-calcium-sodium with mineralization 0.4-0.6 mg/dm3. Total hardness is 6.7-7.3 mol/dm3. Feeding of the complex is being made through the atmospheric precipitates and water inflow from other water-bearing horizons and complexes. Lack of persistent water-proofs at the complex bottom causes hydraulic connection with the waters of Upper Vendian Mogyliv-Podilska Series. The waters are being used by the inhabitants in household purposes. The complex is out of particular value but can be used for centralized water supplying together with the water-bearing horizons in Sarmatian sediments, Obukhivska Suite and Vendian sediments. Water-bearing complex in Upper Vendian Mogyliv-Podilska Series (V2mp) is developed in the south- western part of the area. Water-bearing rocks include sandstones, argillites, aleurolites of 40-50 m total thickness, in places up to 75 m thick. The water-bearing rocks lie over Lower Vendian Volynska Series and are overlain by Cretaceous sediments and water-proof Eocene Kyivska Suite. Water-bearing complex is pressurized. Pressure value varies from 16.0 (DH 64) to 52.0 m (DH 40). Groundwater level depth is +0.76…-34.87 m. Water level altitudes vary from 261.9 to 282.0 m. Water content of the complex is variable. Borehole yields vary from 36.0 to 2298.2 m3/day, specific yields – from 34.7 (DH 943) to 624.5 m3/day (DH 1444). The rock filtration coefficient is 10-20 m/day. Water conductivity of the complex varies in the range from 141 to 988 m2/day. Piezo-conductivity coefficient is 2.3×104-6×105 m2/day. By chemical composition the waters are hydrocarbonate sodium-magnesium-calcium, hydrocarbonate magnesium-calcium-sodium with mineralization 0.4-0.7 mg/dm3. Total hardness is 6.2-9.8 mol/dm3, pH value – 7.3-7.5. Feeding of the complex is being made through the atmospheric precipitates and water inflow from other water-bearing horizons and complexes. Lack of persistent water-proofs both at the complex bottom and top causes hydraulic connection with the waters of adjacent horizons and complexes. The waters of the complex are being used for the centralized water supplying of Khmelnytskiy town. Water-bearing complex in Lower Vendian Volynska Series (V1vl) is developed in the western map sheet part in Volyno-Podilskiy artesian basin. Water-bearing rocks include sandstones, gravelites with tuff-sandstone and tuff-argillite interbeds. Total thickness is 50-60 m, in places up to 100 m. Water-bearing rocks lie over Precambrian crystalline rocks and are overlain by Upper Vendian, Cretaceous and Paleogene sediments. Water-bearing complex is pressurized. Pressure value varies from 18.0 (DH 591) to 62.0 m (DH 306). Groundwater level depth is +1.8…-62.8 m. Water level altitudes vary from 251 to 281 m. Water content of the complex is variable. Borehole yields are from 41.47 to 1728 m3/day, specific yields – 1.15-173.7 m3/day, and in DH 308 – 794.1 m3/day. The rock filtration coefficient is 10-20 m/day. Water conductivity of the complex is 650-690 m2/day. Piezo-conductivity coefficients are mainly 1.69×106 m2/day, and in DH 306 – 9.3×105 m2/day. By chemical composition the complex waters are sulphate-hydrocarbonate calcium-sodium, hydrocarbonate calcium-sodium, sulphate-hydrocarbonate magnesium-calcium, hydrocarbonate sodium with mineralization 0.5-0.7 mg/dm3. Total water hardness is 0.5-9.0 mol/dm3, pH – 7.4-8.1. Feeding of the complex is being made through the atmospheric precipitates and water inflow from other water-bearing horizons and complexes. Lack of persistent water-proofs both at the complex bottom and top causes hydraulic connection with the waters of adjacent horizons and complexes. The waters of the complex are being used for the centralized water supplying of Starokostyantyniv town. Water-bearing complex in fracturing zone of Archean-Proterozoic crystalline rocks and their gruss weathering crust (AR-PR1). Water-bearing rocks include granites, migmatites, gneisses and products of their decomposition – gruss. Since water-baring horizons in the zone of crystalline rocks fracturing and gruss are hydraulically inter- connected, they are combined in the common water-bearing complex. Crystalline rocks are exposed at the surface in the valleys of Sluch and South Boug rivers.

124 In the far north-eastern map sheet part crystalline rocks are overlain by parti-colored clays, Neogene Novopetrivska Suite and Paleogene Buchatska Series. In the central and eastern map sheet parts crystalline rocks are overlain by Quaternary and Neogene sediments, and in the western slope – Paleogene, Cretaceous and Vendian rocks. In the central and eastern map sheet parts, at the watershed slopes, the sequence of primary kaolines is developed which lies over crystalline rock gruss and comprises water-proof. Thickness of the sedimentary cover varies in wide range depending on the crystalline basement and surface relief; thus, the depth of water-bearing complex varies from 1.4 m (Lyubar village) to 110 m (Parkhomivtsi village), and in the far south-west of the area attains 200 m. Normally the waters of given complex are pressurized because of high enough feeding region position relatively to borehole location and development of water-proof clayey sediments or primary kaolines at the top of water-bearing rocks. Somewhere pressure origin is facilitated by the crack sealing with clayey material. Pressure height varies in the range from 1.0 to 66.0 m (Krasnosilka and Tereshpil villages respectively). Water levels are established at the depths from +0.5 (Vel. Mytnyk village) to 65 m (Syomaky village). Fracture water level altitudes vary from 222 to 275 m and value decreasing is observed towards the river and big gully valleys. In places of lacking upper water-proof the waters of the complex are in the direct hydraulic connection with the waters of overlaying water-bearing horizons and surface waters. Water content of the complex is irregular and depends on some natural factors. The highest water content is noted in tectonic zones. Direction of the latter coincides with the direction of river and big gully valleys. Borehole yields vary from 34.6 m3/day under level depression by 40.0 m (Lozova village) to 1105 m3/day under level depression by 17.4 m (DH 977, Lyubar village). Specific yields are 0.9-63.5 m3/day. In places of near-surface development the waters of the zone of crystalline rock fracturing and their decomposition products are being used by the shaft wells. Daily water yields from wells vary from 0.8 (Gubyn village, well 134) to 1.3 m3 (Verbivka village, well 175). Spring yields vary from 17.3 (Berezna village, spring 25) to 25.9 m3/day (Kumanivtsi village, spring 24). The complex water conductivity varies in the range from 34- 75 to 139 m2/day (DH 976). Piezo-conductivity coefficients are normally in the range 1.0×105-5.0×105 m2/day. By chemical composition the complex waters are hydrocarbonate magnesium-calcium, sulphate- hydrocarbonate magnesium-calcium and sulphate-hydrocarbonate sodium-calcium. Water mineralization varies in the range 0.5-0.9 g/dm3, total hardness – from 5.6 to 12.6 mol/dm3, pH – from 7.2 to 7.8. In Khmelnytske deposit of medial waters at the sites “Lisova” and “Kurortna” the radium content is high enough but not exceeds TAC and is 18.9×10-12 and 19.9×10-12 Ku/dm3 respectively. At the site “Kutortna” uranium content is 0.197 mg/dm3 exceeding TAC in almost 2.5 times. Thus, in general content of mentioned components matches requirements of sanitary-hygienic norms for drinking waters, except “Kurortna” site of Khmilnytske deposit of mineral radon waters. Feeding of the complex is mainly being made through the atmospheric precipitates and partly by water inflow from overlaying water-bearing horizons in cases of lacking upper water-proof. The feeding regions are located both in the map sheet area and outside. The water-bearing complex is being discharged in the river and big gully valleys in the springs and hidden groundwater discharge directly into the river courses, and partly into the overlaying water-bearing horizons. The longstanding system observations, performed by Podilska GE in the map sheet area, confirm fracture water level regime dependence on meteorological factors. Annual variation amplitude in boreholes in places of near-surface location of water-bearing complex attains 0.8 m, and with crystalline rock descending beneath sediments it decreases to 0.2-0.4 m. Water-bearing complex of the zone of fractured crystalline rocks and their weathering crust is being widely exploited by single boreholes and their groups for water supplying of agricultural objects, industrial enterprises and some inhabited localities. It comprises one of the major sources of the centralized water supplying.

125

109. MINERAL RESOURCES AND REGULARITIES IN THEIR DISTRIBUTION

The studied area, according to the scheme of zonation, accepted for the Complex metallogenic map of Ukraine in the scale 1:500 000, 2003, is located in the western part of the Ukrainian Shield metallogenic province. Far western map sheet part belongs to Volyno-Prychornomorska metallogenic province. In the Ukrainian Shield province most part of the map sheet territory belongs to Podilska tectonic-metallogenic zone (TMZ) of Dnistersko-Buzka sub-province, and just the far north-north-western part – to Zhytomyrska TMZ of Volynska sub-province. Podilska TMZ includes Khmilnytska and Khmelnytska metallogenic zones (MZ) which coincide with the same-named tectonic structures of the north-western and sub-latitudinal extensions respectively. In Khmilnytska MZ, in the map sheet area Makharynetske and Bratalivske ore-bearing fields are distinguished with specialization for graphite and molybdenum, and Khmilnytske one specialized for radioactive elements and rare-earths. In the far north-eastern map sheet part Veselkivske graphite-bearing field is distinguished. In Khmelnytska MZ, in the map sheet area Goloskivske, Antonivske and Rudnyanske ore-bearing fields are distinguished, specialized for apatite and rare-earths. After results of EGSF-200, Grytsivske ore-bearing field is distinguished in Zhytomyrska TMZ with vermiculite specialization. Volyno-Prychornomorska metallogenic province is represented by Prypyatsko-Dnisterska TMZ. Metallogeny in this part of the territory is weakly studied. Discovery of chalcosine mineralization in Vendian sediments confirms the general specialization for copper in this TMZ.

39Combustible mineral resources

76Solid combustible minerals

109Peat

Peat bodies in the studied area are confined to the flood-lands of South Boug, Khomora, Sluch rivers and their branches. The lowland valley and flood-land peat deposits are developed, normally extended along rivers in the narrow bands up to 1 km wide and up to tens of kilometers long. The map sheet territory belongs to the forest-steppe peat region. Most its part is occupied by Podilskiy forest-steppe area, and the eastern map sheet part – Pravoberezhniy Prydniprovskiy steppe area. In Podilskiy area the multi-layer bog, cane, much rarely multi-layer forest-bog, bog-forest, sedge peat bodies are observed. Peat decomposition degree is mainly medium. Ash content is very high, which is related to the feeding conditions, river flooding and deluvial removal. Peat is mudded therein, penetrated by lime, in places with sand admixture. The mineral interbeds are observed in the bodies, and mineral overburden up to 1 m thick. In Pravoberezhniy area peat bodies are mainly cane, in places with minor bottom layer of bog-forest peat and surface bog-sedge, sedge peat. Peat decomposition degree is mainly medium. Ash content is high because of peat deposits location in flood-lands, peat is mudded, with sand. In the map sheet area 33 peat deposits are located (Annex 2). Peat deposits are from 25 to 1630 ha in size, of these almost 50% - from 25 to 100 ha; two deposits only are more than 1000 ha in size: Buzhanske (I-2-72) and Vovkivske (IV-3-128). Peat differs in high ash content – 15.7-53.7%. The depth is 1.0-4.8 m. The state of peat mineral-resource base is being periodically evaluated in geological-economic reviews (1996, 1998, 2003) of SE “Pivnichgeologia”. In the review of 2003 [57] detailed information is given concerning reserves, exploitation progress, and directions of use. Most of deposits had been being mined by the local inhabitants and industry. At present only one deposit is in production – Voytivetske (III-4-111). Peat is being used as fertilizer and fuel.

126

40Metallic mineral resources

77Non-ferrous and base metals

110Nickel

Zhdanivskiy complex occurrence (III-4-149a) of nickel, cobalt, copper and chromium with concomitant precious metal mineralization is related to the same-named intrusive massif about 350×150 m in size. In the cross-section the massif look like overturned irregular cone with steeper eastern contact. Maximum identified vertical thickness is 170.0 m. The massif is composed of serpentinized peridotites and pyroxenites with nontronite weathering crust up to 50 m thick developed above. The massif is studied by mapping drill-holes conducted by Pravoberezhna GE in the course of prospecting works for diamonds and three structure-mapping drill-holes in the course of EGSF-200. Of the valuable components, nickel is the major one in term of grade and persistent distribution in the column. The persistent nickel content 0.1% (maximum – 0.347%) is observed in the nontronite weathering crust, serpentinites and peridotites in the massif western flank. In the central part just in weathering crust nickel content is about 0.15%, highest – 0.524-1.617%. In the eastern massif flank only in serpentinites, in the upper layers of weathering crust, and in peridotites of the bottom part, the nickel content is 0.15-0.3% in average (maximum – 0.809%). The same are intervals the most persistent and highest cobalt contents (0.01-0.08%) and chromium (up to 0.4%) confined with. Copper content at the levels of tenth percentage is noted in serpentinites. After mineralogical analysis, ore minerals include chromite, chalcopyrite, chalcosine, native copper, pyrrhotite, pyrite, as well as magnetite and ilmenite. In view of small object size and low enough content of mentioned metals, the given occurrence cannot be assessed as perspective. In the studied of core sections from mapping drill-holes increased precious metals concentrations were determined and platinoid mineral-carrier was identified – sperilite. After results of sample analysis from structure-prospecting drill-holes the highest platinoid content is 0.79-2.45 g/t, including platinum – up to 0.11 g/t, palladium – up to 1.2 g/t, ruthenium – up to 1.09 g/t; highest gold content – 0.36 g/t, silver – up to 17-22 g/t. These results, especially sperilite mineral finding, are first positive for platinoids ones in the given area. In the next geological works attention should be focused on the possible discovery of minor ultramafic massifs perspective for precious metals prospecting, platinum first of all.

111Titanium

Titanium occurrences in the studied area are only noted in the weathering crust of crystalline rocks in Antonivske and Goloskivske ore-bearing fields. Ilmenite content, after mineralogical analysis, varies from 36.3 to 61.6 kg/m3. Suslivtsi occurrence (IV-3-162) is located in Antonivske ore-bearing field. It is confined to the weathering crust of charnockites and enderbites. Occurrence is extended in sub-longitudinal direction by 360 m. Overburden rock thickness is 17-18 m, thickness of ore body is from 3.0 to 7.5 m. After mineralogical analysis, ilmenite content is from 52.3 to 61.6 kg/m3. Verbky occurrence (IV-3-165) is located in Antonivske ore-bearing field. It is confined to the gruss weathering crust of quartz syenite. Thickness of productive interval is from 5.0 to 6.5 m, overburden thickness – from 29.0 to 44.0 m. After mineralogical analysis, ilmenite content is from 36.3 to 61.6 kg/m3, zircon – 3.74 kg/m3. Rusanivtsi occurrence (IV-2-155) is located in Goloskivske ore-bearing field. It is confined to gneiss weathering crust. Thickness of productive interval is 6.0 m, overburden rock thickness – 9.0 m. After mineralogical analysis, ilmenite content is 44.22 kg/m3. Increased concentrations of titanium-bearing minerals in the rocks of sedimentary cover are related to erosion of ilmenite-bearing mafic and ultramafic rocks of Sabarivskiy, Proskurivskiy, dyke complexes, meta- basites of Dnistersko-Buzka Series and, probably, ilmenite-bearing sand sediments of Novopetrivska Suite developed to the north-east from the studied area. They are noted in sandy sediments of Buchatska Series, the basal horizon of Kyivska Suite, and in the Miocene sequence of coaliferous sands and clays.

127

78Rare metals

112Molybdenum

Three molybdenum occurrences are discovered in the studied area located in the zone of Khmilnytskiy fault (north-eastern branch) and related to three massifs of Litynskiy complex charnokitoids of granodiorite composition – Malobratalivskiy, Kovalenkivskiy and Lyubarskiy. Malobratalivskiy occurrence (I-4-13) is encountered in the course of DGM-200 [47] and then studied during GM-50 [44] and DGM-50 [13]. Occurrence consists of three blocks: Malobratalivskiy itself, its south- eastern flank, and Lysogirskiy. The first one is best studied. Within high-contrasted molybdenum geochemical anomaly 1.6 km2 in size in 6 from 18 mapping and structure-prospecting drill-holes the ore bodies are intersected with molybdenum content 0.04% and higher. Ore bodies comprise the stock-like mineralized zone consisting of 1-3 sections enriched in molybdenite. Mineralized zone is confined to tectonically modified and metasomatically altered (mainly K-feldspatized) biotite-hypersthene and biotite-amphibole-pyroxene granitoids of granodiorite composition. It is controlled by flat fault which complicates the north-eastern branch of Khmilnytskiy fault. Kovalenkivskiy occurrence (I-4-142) is encountered in the course of GM-50 [44]. It is confined to coarse-grained charnockites. Slight microclinization and amphibolization are observed in occurrence. Molybdenum content in some samples is from 0.057 to 0.19%. The length of potentially ore zone by periphery is about 8 km.

79Precious metals

113Gold

The sign-kind gold content in sedimentary rocks is defined by mineralogical analysis in coastal-marine Sarmatian (I-3-6, I-3-8, II-2-24, III-3-33), Obukhivski marine (II-2-18) and Quaternary sediments – in alluvium of the first-second over-flood terrace (I-3-79) and in modern alluvium (II-2-88, II-3-91). Mineral form is native gold. Gold content is one-two signs. The grains are up to 0.15 mm in size, platy, with shaggy surface, goldish- yellow. In the crystalline rocks, in Kudynka village area, the planar geochemical gold anomaly is distinguished with gold content 0.2 g/t and silver up to 2 g/t [51]. It is confined to the zone of silicification and sulphide mineralization in graphite-biotite gneisses of Bereznynska sequence. Increased precious metal concentrations (platinoids, gold and silver) are identified in Zhdanivskiy complex occurrence.

80Rare-earth metals

114Monazite

Increased rare-earth metal content in the studied area is mainly related to monazite mineralization. Monazite comprises accessory mineral in almost all granitoids of the area. High rare-earth concentrations are identified in pegmatoid granites and pegmatites of Khmilnytskiy complex, metasomatically altered granitoids of Berdychivskiy complex in Khmilnytska metallogenic zone. In the area eight monazite occurrences are identified: Dibrovka (III-4-150), Markivtsi (IV-3-163), Rozhny (III-3-148), Shrubkiv (IV-2-154), Suslivtsi (IV-3-159), Shchedrova (IV-3-160), Bokhny (IV-3-167). Of these, Dibrovka, Markivtsi and Suslivtsi occurrences are most perspective. Dibrovka occurrence (III-4-150) is located at the north-western outskirt of Dibrovka village. It is confined to weathering crust of cataclased biotite granitoids. Monazite content, after mineralogical analysis, is 11.4 km/m3. Suslivtsi occurrence (IV-3-159) is located in Antonivske ore-bearing field in 2.5 km to the north-east from Suslivtsi village. It is confined to the gruss weathering crust of pyroxene syenite (melteigite?). After mineralogical analysis, monazite content is 7.26 kg/m3. Markivtsi occurrence (IV-3-163) is located to the south from Markivtsi village. After mineralogical analysis, in feldspar-quartz fine-medium-grained sand monazite content is 5.08 kg/m3, ilmenite and leucoxene – 9.2 kg/m3, garnet – 23.48 kg/m3, as well as minor zircon, pyrite, apatite and collophane, staurolite and kyanite- group minerals.

128

81Radioactive metals

115Uranium, thorium

In the studied area eight radioactive element occurrences are identified: Zhdanivka (III-4-149), Sokolova (III-4-151), Veselka (I-4-139), Goloskiv (IV-2-156), Suslivtsi (IV-3-158), Bokhny (IV-3-167), Lelitka (IV-4-168), Dyakivtsi (IV-4-169). Occurrences contain both thorium and uranium mineralization. Of these, Zhdanivka and Sokolova occurrences are most perspective. Zhdanivka occurrence (III-4-149) is identified by Pravoberezhna GEE in 2001-2002 in the course of prospecting for diamonds and then it was studied during EGSF-200. Occurrence is confined to the exo-contact zone of ultramafic massif with host granitoids of Berdychivskiy complex. Uranium mineralization is directly related to albite metasomatites. After X-ray-spectral analysis, uranium content is 0.0733-0.0893%, thorium – 0.0098-0.0126%. Occurrence is recommended for specialized prospecting works. Sokolova occurrence (III-4-151) is identified during complex study of Khmilnytske deposit of radon mineral waters in 1966-1967. It is located in 1.0 km to the north-west from Sokolova village. After gamma- spectral analysis, uranium content is up to 0.042%.

41Non-metallic mineral resources

82Ore-chemical raw materials

116Agro-chemical raw materials

Apatite

Increased phosphorus concentrations are related to apatite mineralization in crystalline rocks and their weathering crusts and with collophane mineralization in the basal horizon of Obukhivska Suite sediments. In Pylypchanska Suite sands they are related to glauconite. After GM-50 data [51], sub-latitudinal Khmelnytska metallogenic zone is distinguished comprising metallogenic expression of the same-named tectonic zone. The zone is specialized for apatite and rare earths; it is more than 40 km long and 15 km wide. In the crystalline rocks and their weathering crust apatite ore concentrations are indentified in the intrusive rocks of alkali-gabbroid formation (Paleo-Proterozoic Proskurivskiy complex): pyroxenites, gabbro and gabbro-norites, alkali gabbroids (shonkinites), syenites. The faults of sub-latitudinal Khmelnytska zone had played magmo- and ore-feeding functions. Intrusive bodies are often located at the cross-junctions with the north-west-trending faults which apparently are ore- containing. In Khmelnytska metallogenic zone Goloskivske ore field, Antonivske and Rudnyanske ore-bearing fields where the massifs and minor bodies of alkali-gabbroid formation are concentrated. Goloskivske ore field occupies the northern part of Medzhybizkiy enderbite-gneiss dome located in Khmelnytska tectonic zone. The dome structure is mainly composed of Paleo-Archean pyroxene mafic gneisses of Tyvrivska sequence of Dnistersko-Buzka Series, and gneiss-like enderbites of Gayvoronskiy complex. These rocks underwent charnockitization in Meso-Archean and granitization in Paleo-Proterozoic, and at about 2 Ga were intruded by mafic magma enriched in phosphorus. In the ore field Goloskivskiy occurrence of apatite ore is identified, as well as some points of increased apatite mineralization, planar geochemical phosphorus aureoles in the crystalline basement rocks and their weathering crust. Apatite occurrences (IV-2-65; IV-2-56) and points of increased mineralization are related to apatite re- deposition in the basal horizon of Eocene Obukhivska Suite providing prospecting criterion for the bed-rock ores. In addition, occurrences (IV-2-53; IV-2-54) of collophane mineralization in Cretaceous sediments (Pylypchanska Suite) are encountered. The ore field is about 90 km2 in size. Goloskivske apatite ore occurrence (IV-2-157) is located in 2 km to the south-west from Goloskiv village and confined to the same-named gabbroid massif 1400×150×300 m in the plane with maximum vertical thickness 150 m.

129 According to data available, the massif comprises layered intrusion composed of apatite-bearing meso- and leucocratic biotite gabbro-norites and norites in the central part, and melanocratic biotite-amphibole gabbro and pyroxenites at the margins with higher apatite content than in the rocks of central part which are considered to be the ore body in the massif’s geological boundaries. In the bed-rocks average P2O5 content is 4.9%, maximum – 10.5%. In the samples from weathering crust of mafic rocks P2O5 content is as follows: 6.0% over thickness 10.0 m; 6.62% over 4.5 m; 6.93% over 4.0 m; 8.16% over 3.0 m. After mineralogical analysis, increased apatite content is identified. High apatite concentrations are identified in the basal horizon of Obukhivska Suite which overlies the massif rocks. Like the friable ores of weathering crust, apatite-bearing rocks of basal horizon can be exploited at the bedrock object mining. In the ores of Goloskivskiy occurrence content of other ore components is low, titanium first of all, whose pentoxide content varies from 0.96 to 1.36%, rarely attaining 2%, and in this respect this occurrence differs form the known apatite-ilmenite deposits of Ukrainian Shield. Prospecting works continue in the field. Antonivske ore-bearing field is the area of wide development of alkali-gabbroid formation intrusive rocks. The biggest massifs (Antonivskiy and Verbkivskiy) are located at the cross-junctions of the magma- feeding sub-latitude faults of Khmelnytska tectonic zone and the north-western faults. The minor bodies are mainly confined to sub-latitudinal faults. The intrusive rocks constitute the range: essexites – ijolites – nepheline syenites – alkaline syenites – syenites and quartz syenites. Intrusions are accompanied by phenite and phenitized rock aureoles. Geochemical specialization for phosphorus and available apatite mineralization are characteristic for all rock varieties. The highest apatite concentrations are noted in alkaline and sub-alkaline gabbroids. In the ore field Verbkivskiy apatite ore occurrence in shonkinites is encountered, as well as the points of increased apatite mineralization in pyroxene syenites and sub-alkaline gabbroids. Besides phosphorus, rare-earth increased concentrations are also noted. Antonivske ore-bearing field is 75 km2 in size. Verbkivskiy apatite ore occurrence (IV-3-166) is discovered in the course of GM-50 [51]. Intersected massif of alkaline rocks is mainly composed of biotite-pyroxene shonkinites alternating with pyroxene-biotite syenites and orthoclase pyroxenites. All rocks are apatite-bearing. Content of P2O5 (chemical analysis) varies from 1.06 to 4.5%. The massif is extended in the north-western direction by 1.2 km being 200-450 m wide and located in 3.2 km to the south-west from the biggest in the area Antonivskiy massif of alkaline rocks. In the rocks of Antonivskiy massif high apatite concentrations are not identified but taking into account the rock variability, including wide development of main alkaline and sub-alkaline rocks, discovery of blocks with economic apatite concentrations seems quite possible in the massif. Rudnyanske ore-bearing field is weakly studied. Alkali-gabbroid formation massifs are confined to the cross-junction of sub-latitudinal breaks of Khmelnytska tectonic zone and the north-western Rudnyanskiy fault; the rocks are developed in the site 25 km2 in size. Increased content of phosphorus-bearing minerals in the rocks of sedimentary cover is noted in Cretaceous Pylypchanska Suite and Eocene Obukhivska Suite. In the rocks of sedimentary cover 4 occurrences and 2 points of increased mineralization are distinguished which are located in the western part of studied area in Goloskivske ore field. Pyrogivskiy occurrence (IV-2-53) is located in 0.5 km to the east from north-eastern outskirt of Pyrogivtsi village. In the fine-micro-grained quartz-glauconite sands of Pylypchanska Suite with coarse flint nodules P2O5 content is 3.16-6.74%. Thickness of phosphorus-bearing layers varies from 3.0 to 5.7 m, average – 3.9 m; depth is from 36.4 to 43.5 m, average – 38.2 m. In the underlaying sediments of Pylypchanska and Grushkivska suites, and also in the rocks of crystalline basement increased content of phosphorus-bearing minerals is not identified. High phosphorus content is related to collophane mineralization. Goloskivskiy occurrence I (IV-2-54) is located in 2 km to the south-west from south-western outskirt of Goloskiv village. By chemical analysis of the fine-micro-grained quartz-glauconite sand of Pylypchanska Suite with flint nodules P2O5 content is estimated to 3.42-5.82%; it is apparently related collophane mineralization and probably partly with apatite input from disintegration zone of apatite-bearing crystalline rocks. Thickness of the layer varies from 1.0 to 4.0 m, in average – 2.5 m. In the underlaying sediments of Grushkivska Suite, crystalline basement rocks and their weathering crust phosphorus is not identified. Goloskivskiy occurrence III (IV-2-55) is located in 1.5 km to the south-west from Goloskiv village. Occurrence is confined to the field of Goloskivskiy apatite occurrence in crystalline rocks. By chemical analysis, in the fine-medium-grained glauconite-quartz sands and in the basal horizon of Obukhivska Suite, composed of sandy-clayey sediments with gruss of quartz, feldspar and basement rocks as well as admixture of re-deposited

130 weathering crust, P2O5 content is 0.49-8.42%; average thickness of phosphorus-bearing layers is 3.5 m, average depth – 22.1 m. It should be noted that higher content (3.68-8.42%) is noted in quartz-glauconite sands overlaying as weathering crust as the basal horizon, whereas in the basal layer P2O5 content varies in the range 0.49-1.38%. The given occurrence is developed through re-deposition of apatite from supergene zone of apatite- bearing gabbroids.

117Raw materials for soil chemical improvers

Limestone

In the studied area one limestone deposit is explored suitable for soil chemical improvers. Sakhnovetske deposit (II-2-21) is 4.3 ha in size and located at the southern outskirt of Sakhnivtsi village. The raw materials are organogenic-detritus, dense, often re-crystallized limestone. Limestone average thickness is 9.74 m, overburden rocks – 1.0 m. The raw materials are suitable for lime powder and construction lime manufacturing. Reserve growth is possible in the south-western direction and to the depth.

83Non-metallic ore raw materials

118Electric- and radio-technical raw materials

Graphite

In the studied area graphite occurrences are confined to the batches of graphite-bearing gneisses of Bereznynska sequence. In ultra-metamorphic rocks (charnockitoids, granitoids) graphite is observed in fine-flake varieties and is out of practical value. In the map sheet M-35-XXII eight graphite occurrences are encountered and in one of these (Makharynetskiy) prognostic resources are evaluated. Makharynetskiy occurrence (II-3-144) is located in 0.5 km to the south-east from Makharyntsi village. It is confined to graphite-biotite gneisses of Bereznynska sequence. Ore body comprises a bed of complex structure. The strike is west-north-western and dipping angle ~45o to the north-north-west. Thickness of ore body is 160-550 m, the length (by geophysical data) is ~1.8 km, depth from the surface – 0-13 m. It is studied to the depth 210.0 m. Average free carbon content in occurrence is 4.83%.

119Adsorption raw materials

Vermiculite

Brazhynetskiy occurrence (I-3-135) is encountered at the stage of EGSF-200. In the studies of local gravity maximum 2 mGal in amplitude, which coincides with low-intensity (φo = -0.8o) electric polarization anomaly, in drill-hole conducted in 2.7 km to the south-east from the eastern outskirt of Brazhyntsi village, the hydromica weathering crust is intersected, developed above melanocratic gabbro-monzonites. In the hydromica, economic vermiculite concentrations are identified (13.0-22.38%) with average content by the ore interval 17.69%. Thickness of overburden rocks is 25.7 m. Brazhynetskiy gabbro-monzonite massif is confidently mapped by geophysical data; it is about 2.6 km2 in size and extended over 2 km to the north-west and north being 1.3 km wide. Mineral composition of the ores: phlogopite, hydro-biotite, vermiculite, plagioclase, amphibole. Vermiculite ores are observed both in bunches and lenses in the zones of secondary shearing and in pods disseminated over entire rock mass. Mica development in the massif is related to potassium metasomatism. Vermiculite properties include: high heat- and sound-proof, fire-proof, adsorption and catalysis, high chemical resistance, decorative, lightness, elasticity, swelling capacity; these allow its using for the steam line heat-proofing in the energy and cooling devices, thermal-electric equipment in metallurgy, foundry manufacturing, chemical industry, agriculture and construction materials manufacturing. To date no vermiculite deposits are in production in Ukraine. According to recent data, vermiculite price at New York stock exchange and in South Africa is 180-230 USD per ton.

131

120Facing stone raw materials (decorative stone)

Granite, charnockite

In the studied area the granitoids of Berdychivskiy and Litynskiy complex are most developed. Low depth and thin overburden along the major river valleys provide favorable conditions for prospecting of granitoids as the facing and block stone raw materials. To date in the mapped area prospecting works are conducted in Popivetske and Kudynske facing stone deposits described below. Popivetske deposit (IV-3-60) is located in 1.5 km to the south-west from Popivtsi village. Deposit is studied by Kyivska prospecting group of Pravoberezhna GE in 1984-1986 in the course of prospecting for block stone. Explored area is 15.59 ha. The raw materials are charnockites of Litynskiy complex; explored thickness is 40.3-42.2 m; overburden thickness – 6.5-9.5 m. The raw materials are suitable for block manufacturing. Assumed block output is 20-25%. The wastes are suitable for crushed stone manufacturing. Kudynske deposit (III-3-57) is located in 1.1 km to the north-east from Kudynka village. Deposit is encountered by Kyivska prospecting group of Pravoberezhna GE in 1984-1986. Explored square is 4.46 ha. The raw materials are granites of Berdychivskiy complex; explored thickness is 20.0-34.0 m, overburden thickness – 16.0-30.0 m. The raw materials are suitable for block manufacturing. Assumed block output is 20-25%. The wastes are suitable for crushed stone manufacturing.

121Glass and porcelain-faience raw materials

Primary kaoline

Primary kaoline constitutes weathering crust of crystalline rocks. In the studied area kaoline exposures are mainly observed in the eastern part. Three occurrences of primary kaolines are encountered in the territory. Rogoznynskiy occurrence (II-3-145) is located in the area of Ozharivka and Rogizna villages. Occurrence is discovered in the course of GM-50 [13]. Kaoline is intersected at the depth 10.7-19.0 m. Primary kaoline is developed after migmatites and biotite granites. Occurrence is 5.7 km2 in size. Thickness of kaolines is 2.2-13.5 m. According to the studies of predecessors, primary kaolines are low-grade and can be used for refractory materials manufacturing. This occurrence is perspective and requires further studies. Velyki Derevychi occurrence (I-3-134) is located in 1 km to the north from northern outskirt of Velyki Derevychi village. Quartz-kaolinite weathering crust is developed after biotite gneisses with minor bodies of leucocratic pegmatoid granites. Kaoline is intersected at the depth 12-20 m. Occurrence is about 2 km2 in size, average thickness of productive horizon is 5.0 m. Occurrence is located on the arable lands. Avratynskiy occurrence (I-4-143) of kaolines is located at the north-eastern outskirt of Avratyn village. Occurrence is encountered in the course of GM-50 [44]. It is confined to granite weathering crust. Kaoline is intersected by minor quarries at the depth 0.6 m. The raw materials are being used by the local inhabitants.

84Construction raw materials

122Petrurgy and light concrete filler raw materials

Claydite

In the studied area Middle Sarmatian clays are widely developed. They were studied for suitability of claydite manufacturing. After laboratory analysis data, the clays do swell well enough under 1% addition of straw oil and are suitable for claydite manufacturing. The clay is yellowish-grey, yellow, brown, greenish-grey, in places dark-grey to black, in places sandy, with sand interbeds, at the bottom aleuritic, somewhere coaliferous. Thickness of clays is from 28.0 to 39.3 m. Overburden thickness is 1.0-8.5 m.In the studied area four occurrences are distinguished: Gromivka (II-2-19), Reshnivka (II-2-20), Illyashivka (II-2-25), Zagirne (II-3-29).

132

123Construction lime and gypsum raw materials

Limestone

In the studied area carbonate rocks are widely developed and include Eocene marls of Kyivska Suite and Miocene limestones. In practical respect, as the carbonate raw materials for lime manufacturing, the detritic, oolite-detritic and organogenic-detritic limestones are of interest. Their numerous surface exposures are observed by both banks of major rivers. In the mapped territory Grytsivske (I-1-2), Vesnyanske (II-2-23) and Trebukhivetske (IV-2-51) deposits of carbonate raw materials for lime manufacturing are located. Grytsivske deposit (I-1-2) is located in 1.4 km to the south-east from Koskiv village. The square is about 4.0 ha. The raw materials are Sarmatian dense limestones. Average thickness of limestones is 2.9 m, overburden rocks – 2.3 m. After results of chemical analysis, limestone is suitable for the air construction lime manufacturing. Vesnyanske deposit (II-2-23) is located in 1.6 km to the north-east from Vesnyanka village. Square is 5.8 ha. The raw materials include Sarmatian limestones: oolitic, re-crystallized (upper layer) and shell, very strong (lower layer). Average thickness of both layers is 3.46 m, overburden rocks – 2.4 m. After results of chemical analysis, limestone is suitable for the air construction lime manufacturing. Reserve growth is possible in the eastern direction.

124Quarry-stone (aggregate) raw materials

Granite, limestone

In the purposes of quarry-stone and debris manufacturing Precambrian crystalline rocks are being used – granites and migmatites of Berdychivskiy complex, charnockitoids of Litynskiy and Gayvoronskiy complexes, gneisses and mafic gneisses of Dnistersko-Buzka Series, as well as Sarmatian limestones. The biggest deposits, located nearby Rusanivtsi (IV-2-52) and Golovchyntsi (IV-2-47) villages, are being exploited by automated method. In total, 14 granite deposits and 4 limestone deposits are explored in the area. In Khmelnytska Oblast from 11 granite deposits 3 are in production (Krasnosilkivske, Rusanivske and Golovchynetske), other are out of production or in conservation. Of four limestone deposits three are out of production – Stavnytske (IV-2-46), Golovchynetske (IV-2-47), Terlivske (IV-3-63). In Rusanivske deposit (IV-2-52) limestones are being used together with enderbite-gneisses for 400-class quarry-stone manufacturing, and in Antonivske deposit (IV-3-59) – as the filler for concrete and constriction liquids. Rusanivske deposit (IV-2-52) is located in 0.3 km to the south-east from the southern outskirt of Rusanivtsi village. The raw materials include unaltered and not weathered granitoids (enderbites of Gayvoronskiy complex) and limestones. Granites of Rusanivske deposit are being used for debris and quarry-stone manufacturing. At the sane time, limestones are being mined suitable for quarry-stone manufacturing. Deposit is being mined by open-cast method. Quarry length is up to 350 m, width – up to 200 m, depth – more than 50 m. Quarry consists of 3 benches 10-25 m high each. From the south, east and north arable lands are located, and from the west – the South Boug river flood-land, therefore, reserve growth is only possible to the depth. Antonivske deposit (IV-3-59) is located in 0.8 km to the north-west from Antonivka village. The raw materials are Sarmatian limestones. Under mining limestone can be wetted through atmospheric and flood waters. Explored square is 80 th.m2. The quarry depth is up to the groundwater level. After results of chemical analysis, limestone is suitable for the carbonate sand manufacturing. Reserve growth is possible by means of further exploration in the field to the north and east.

125Brick-tile raw materials

Loams

The brick-tile raw materials in the studied area include Quaternary loams widely developed in the territory.

133 In total, 29 minor deposits are encountered. Of these, three ones are in production: Sakhnovetske (II-2- 89), Parkhomivetske (IV-2-122), Shchedrivske (IV-3-125). Sakhnovetske deposit (II-2-89) is located at the western outskirt of Krasnosilka village, on arable lands 4.5 ha in square. The raw materials are Quaternary loams 3.9 m thick. Thickness of overburden rocks (soil-vegetation layer) is 0.5 m. In laboratory and semi-plant testing it is determined that the mixture of yellow-brown and yellow loams, combined in the proportion to the thickness of layers in geological column, is suitable for the solid construction brick manufacturing by means of ductile compression under conditions of natural drying within 8- 10 days and roasting at the temperature 980oC. Reserve growth is possible in the southern and eastern directions. Deposit is being exploited by Starokostyantynivskiy brick plant producing “75”-class brick. Parkhomivetske deposit (IV-2-122), 4.2 ha in square, is located at the watershed of South Boug and Buzhok rivers, at the south-eastern outskirt of Parkhomivtsi village. The raw materials include all varieties of loams and clays. The total average thickness is 6.7 m. The overburden rocks consist of the soil-vegetation layer. Hydrogeological conditions are suitable: there are no water-bearing horizons within productive sequence. The clays and loams are suitable for solid construction brick manufacturing by means of ductile compression in the mixture, combined in the proportion to the thickness of layers in geological column, under conditions of natural drying within 12 days and roasting at the temperature 980oC. Reserve growth is possible in the south-western and south-eastern directions. Shchedrivske deposit (IV-3-125) is located at the north-eastern outskirt of Shchedrova village. The raw materials include two loam varieties, light-brown and yellow ones. The total average thickness is 9.8 m. Thickness of overburden rocks (soil-vegetation layer) is 0.9 m. Deposit is not watered. It is determined that light- brown loam, in pure state and in mixture with yellow loam (in proportions 50:50 and 80:20), is suitable for the solid “100”-class and MRZ-25 brick manufacturing under natural and artificial drying conditions of raw brick mass. Reserve growth is possible in the northern and north-eastern directions in arable lands.

42Waters

85Groundwaters

The territory of map sheet M-35-XXII is well supported with high-quality groundwaters. The major source for water supplying of towns, industrial and agriculture enterprises, and farms, are groundwaters of water-bearing horizons in Sarmatian sediments, Lower and Upper Vendian Volynska and Mogyliv-Podilska series, and fracturing zone of Precambrian crystalline rocks and their gruss weathering crust. The rural inhabitants do mainly use the waters of the first from the surface water-bearing horizons which not always match the sanitary-hygienic requirements.

126Fresh waters

For the water supplying of Starokostyantyniv and Stara Synyava towns, at the sites KECH and “Mysyurivska”, deposits are explored and fresh groundwater reserves are approved in the Sarmatian water- bearing complex; both objects at present are in exploitation. By chemical composition the waters are sulphate- hydrocarbonate magnesium-sodium and hydrocarbonate magnesium-calcium. The water quality matches State Standard 2872-82 “Drinking water”. For the water supplying of Khmelnytskiy town the fresh groundwater reserves are explored and approved for water-bearing complex in Upper Vendian Mogyliv-Podilska Series sediments at the operating water-scoops “Tsentralniy” and “Kudrynka” and undeveloped Pyrogivska site. Besides that, reserves and explored and approved at the site “Pashutynska” (for water-bearing complexes in Upper Cretaceous Ozarynetska and Pylypchanska suites, and Upper Vendian Mogyliv-Podilska Series) which at present is out of exploitation. By chemical composition the waters are hydrocarbonate magnesium-sodium-calcium and hydrocarbonate magnesium-calcium-sodium with mineralization 0.4-0.7 mg/dm3. Fresh groundwater reserves are explored and approved for water-bearing complex in Lower Vendian Volynska Series at the sites “Grygorivska” and “Pashkivetska”, which are being exploited for water supplying of Starokostyantyniv town. By chemical composition the waters are hydrocarbonate magnesium-calcium-sodium and sulphate-hydrocarbonate magnesium-sodium-calcium with mineralization 0.5-0.7 mg/dm3.

134 Fresh groundwater reserves are explored and approved for water-bearing complex in fractured zone of Precambrian crystalline rocks and their gruss weathering crust for centralized water supplying of Khmilnyk town (“Sydorivska” site), Lyubar minor town (“Markivska” site), and animal farm in Popivtsi village of Letychivskiy area. All three deposits at present are out of exploitation. By chemical composition the waters are hydrocarbonate magnesium-calcium and sulphate-hydrocarbonate sodium-calcium with mineralization 0.5-0.9 mg/dm3.

127Mineral waters

In the map sheet area, nearby Khmilnyk town, the curative resort is operating which uses mineral radon waters in medical purposes. Khmilnytske deposit of mineral curative waters is explored with approved reserves. Deposit is confined to the water-bearing complex of Precambrian fractured crystalline rocks and their gruss weathering crust and consists of four sites: Kurortna, Lisova, Golodkynska and Ugrynivska. By chemical composition the waters are hydrocarbonate calcium and sulphate-hydrocarbonate sodium-magnesium-calcium with mineralization 0.5-0.9 mg/dm3. Content of radioactive components: uranium - <0.002-0.013 mg/dm3, radium – from 1×10-12 to 19.9×10-12 Ku/dm3. Radon waters of Khmilnytske deposit are related with the fault zone of north-western extension where mineral waters with increased radioactivity are being circulated by fractures.

43Regularities in distribution of mineral resources

After results of metallogenic analysis, all available deposits and occurrences are classified by genetic types and ore formations. Relationships of these objects and points of increased mineralization with particular rock complexes are established. Prospecting evidences are also defined indicating perspectives for discovery of various mineral resources in the rocks of crystalline basement and sedimentary cover. For most perspective types of mineral resources metallogenic zonation of the territory is designed and specific metallogenic zones and ore-bearing fields are distinguished.

86Mineral resources in the rocks of crystalline basement and their weathering crusts

The basement metallogeny is defined by the complexity of geological structure and territory relation to mega-blocks developed in various geodynamic environments and complicated by Khmelnytska, Khmilnytska, Teterivska and Andrushivska deep-seated fault zones. Metallogenic features are developed under influence of various metallogenic factors, which are often expressed together, specifically: geodynamic, stratigraphic, magmatic, ultra-metamorphic, metasomatic, and tectonic.

128Metallic mineral resources

Non-ferrous and base metals

In the studied area these include titanium occurrences, discovered in Khmelnytska metallogenic zone, and the complex Zhdanivskiy nickel, cobalt, copper and chromium occurrence in Khmilnytska MZ of Podilska TMZ. These metals, as well as tin, zinc, lead are identified with content which corresponds to the points of increased mineralization and geochemical anomalies. Titanium occurrences are located in Goloskivske and Antonivske ore-bearing fields where sub-alkaline and alkaline mafic rocks are developed. It should be noted that in the mentioned rocks titanium content is relatively low, but titanium re-distribution in the mafic gneisses and melanocratic enderbites, primarily enriched in titanium, can be related to their influence on surrounding rocks and respective accompanied metasomatic processes. The secondary titanium accumulation had occurred in weathering crust. Specifically, Suslivtsi occurrence is confined to enderbite weathering crust in the exo-contact of Antonivskiy massif, and Rusanivskiy occurrence – to weathering crust of Tyvrivska sequence rocks in Goloskivske ore-bearing field. The highest nickel, cobalt and copper concentrations are determined in the rocks of Zhdanivskiy massif in Khmilnytska MZ, first of all in the nontronite weathering crust and serpentinites. The age of this massif is not completely defined although data available allow relation of the massif with tectono-magmatic activization in Khmilnytska fault zone at about 1850 Ma. Discovery of minor massifs or dyke-like bodies of ultramafic rocks is quite possible in this zone.

135 In prospecting respect, Malobratalivskiy molybdenum occurrence is of particular interest; it is located in charnockitoids of Litynskiy complex with evidences for superimposed hydrothermal-metasomatic re- crystallization in the zone of Khmilnytskiy deep-seated fault, at its cross-junction with faults of Bilokorovytska fault zone. The copper, thorium and rare-earth mineralization points and geochemical anomalies are also confined to this cross-junction. Most likely, the north-western faults had played ore-transporting functions whereas sub-longitudinal faults – ore-hosting ones. Apparently, charnockitoids of Litynskiy complex, more mafic in comparison with Berdychivski granitoids, had provided geochemical barrier for precipitation of molybdenum and copper minerals from the silica-potassium hydrothermal solutions. Kovalenkivskiy occurrence is of similar tectonic position and genetic type but it is more distal from the major north-eastern branch of Khmilnytska zone (up to 6-10 km) and molybdenum mineralization is less expressed while increased silver and tin contents are noted among concomitant elements. It can be supposed that charnockitoids of Litynskiy complex along entire extension of Khmilnytska tectonic zone are specialized for molybdenum but low-contrasted geochemical barrier had precluded high-grade ore development.

Rare-earth metals

All rare-earth metal occurrences are related to the rock hydrothermal-metasomatic transformations in the north-west-trending zones of tectonic breaks (Khmilnytska MZ). Identified rare-earth occurrences are caused by increased monazite content in the crystalline rocks and their weathering crusts. In our mind, Suslivtsi occurrence is perspective; it is related to alkaline rocks of Proskurivskiy complex and located in Antonivske ore-bearing field where high (up to 7.26 kg/m3) monazite content is related to the gruss weathering crust of pyroxene syenite.

Radioactive metals

Of the numerous thorium and uranium occurrences, just ones nearby Zhdanivka and Sokolova villages are of practical interest. Both these occurrences are located within Khmilnytskiy massif of leucocratic granitoids and are genetically linked with this massif and tectono-metasomatic activization of the same and even later stages. Most perspective Zhdanivka occurrence is confined to the north-eastern exo-contact zone of Khmilnytskiy intrusive with granitoids of Berdychivskiy complex. The latter in occurrence do contact with ultramafic rocks of Zhdanivskiy massif. Occurrence is located at the cross-junction of the north-western, sub- longitudinal and sub-latitudinal faults. Of these, the north-western faults were probably ore-feeding, and sub- longitudinal fault – ore-hosting. Concerning the latter one, metasomatites of albitite composition with uraninite, uranium black and black uranium oxides are confined to the place where the this fault crosses aforementioned contact with the features of clear geochemical barrier.

Precious metals

To date all perspectives of the territory are related to the identified Zhdanivska intrusion of apo- peridotites-apo-pyroxenites. Increased platinoid content is noted in the contact zones of ultramafic massifs. Relatively low precious metal content and small massif size preclude its assessment as perspective object. Available data, first of all, analysis of large-scale maps of physical fields, do not exclude that other minor massifs of the same composition can be found in Khmilnytska fault zone but with higher concentrations of ore elements.

129Non-metallic mineral resources

Ore-chemical raw materials Agro-chemical raw materials Apatite

All known occurrences of phosphorus raw materials in the studied territory belong to apatite alkali- gabbroid formation. The ore-bearing intrusives are composed of the rock range including pyroxenites, gabbro, gabbro-norites, alkali gabbroids, nepheline syenites, alkaline syenites, syenites and quartz syenites. All these rock varieties contain apatite. Economic apatite concentrations are identified in gabbro, gabbro-norites, pyroxenites, alkali gabbroids (shonkinites). In more felsic rocks P2O5 content attains 3.6%. By the patterns in mineral grains apatite comprises one of the earliest minerals. The intervals are identified with apatite content up to 30% which comprise the primary apatite-pyroxene cumulate.

136 Distribution and localization of intrusive rocks are controlled by tectonic factor, specifically, relation to sub-latitudinal Khmelnytska tectonic zone, where faults had played ore-feeding role. In some cases the massifs and minor fissure intrusions are located at the cross-junctions of these faults by the breaks of north-western extension. Prospecting evidences for the bodies of apatite alkali-gabbroid formation include phosphorus high- contrasted geochemical anomalies (> 0.5-1% after spectral analysis results) in the rocks of crystalline basement, weathering crust, basal horizon of sedimentary cover, apatite occurrence in pan samples after mineralogical studies, as well as apatite observed in thin sections in amount more than 3%. Apatite-bearing massifs and bodies are located in Khmelnytska metallogenic zone, which expresses the same-named tectonic zone, and concentrated in three ore-bearing fields: Goloskivske, Antonivske and Rudnyanske. In the latter, besides apatite, rare-earth specialization is also defined, related to the most felsic rock varieties of alkali-gabbroid formation.

Non-metallic ore raw materials Electric- and radio-technical raw materials Graphite

Identified graphite occurrences are related to gneisses of Bereznynska sequence of Dnistersko-Buzka Series and belong to graphite in gneisses ore formation. Those sequence sections are most perspective in term of graphite which underwent least ultra-metamorphic granitization. These ones include Veselka 1, 2, 3 and Makharyntsi occurrences. Veselka 1-3 ones are confined to the peripheral part of Berdychivskiy block where Bereznynska sequence rocks are widely developed. Similar situation is also observed in Makharynetska site located between two active branches of Khmilnytska tectonic zone, where hydrothermal alteration of Bereznynska sequence gneisses causes graphite re-distribution with coarser flakes development.

Adsorption raw materials Vermiculite

Vermiculite occurrence in the studied area had been encountered for the first time in the course of EGSF-200. Discovery of Brazhynetskiy occurrence, analysis of its tectonic setting, petrological and geophysical parameters made possible definition of the genetic type for prognostic deposit and outlining the area for prospecting works. Vermiculite bodies are related to hydromica weathering crust of gabbro-monzonite massifs developed in Andrushivska deep-seated fault zone. The fields, perspective for vermiculite ores, are related to some massifs, similar to Brazhynetskiy, which are distinguished by geophysical data in Grytsivske ore-bearing field, and also at some sites in Varvarivskiy massif.

Primary kaoline

Kaoline occurrences are noted in the fault influence zones and, respectively, related to these zones linear weathering crusts of granitoids. Rogizna occurrence, located in Bilokorovytska tectonic zone, could be of particular interest.

Facing and construction raw materials

In the facing purposes the Lithynskiy complex charnockites and Berdychivskiy complex granites are being used in the construction industry. Recently decorative properties of Khmilnytski granites from Krutnivskiy quarry were preliminary assessed. All these rocks in the explored sections are weakly fractured and overburden thickness is low therein. All types of crystalline rocks are being used for the quarry-stone manufacturing, as well as limestones if their quality matches needs of the local construction industry.

87Regularities in distribution of mineral resources in sedimentary cover

In case of mineral resources, related to the rocks of sedimentary cover, the major role in localization and control is played by the combined stratigraphic, lithological, litho-facial, paleo-tectonic, paleo-geographic, and geomorphologic prognostic factors.

137 Increased concentrations of ilmenite, zircon, monazite, as well as apatite, depend on litho-facial and paleo-geomorphologic conditions of sedimentation and on abundance of these minerals in the crystalline rocks and their weathering crusts at respective sites. The sites with collophane mineralization are confined to Cretaceous sediments of Pylypchanska Suite. Apatite is commonly concentrated in the basal horizon of Obukhivska Suite in Goloskivske ore field. Ilmenite, zircon and monazite in increased concentrations are commonly observed in the basal horizons of Eocene Obukhivska Suite, Miocene sequence of clays, sands and aleurites, and are also noted in Quaternary alluvial and alluvial-fluvio-glacial sediments. For the sedimentary deposits of construction materials (limestones, claydite, brick-tile loams) the stratigraphic, litho-facial, paleo-geographic and geomorphologic factors are of primary importance. These agents do also control development of peat deposits.

138

1110. ASSESSMENT OF THE AREA PERSPECTIVES

Prognostic assessment of the territory is performed on the ground of complex analysis of metallogenic factors, available prospecting indicators reflecting localization of deposits and occurrences, the industry and agriculture needs in the particular raw materials. Of the identified objects, the territory perspectives are first of all related to the occurrences of uranium (Zhdanivka, Sokolova), vermiculite (Brazhynetskiy occurrence in Grytsivske ore-bearing field), apatite (Goloskivskiy, Verbkivskiy occurrences), as well as graphite, molybdenum, and also deposits of construction materials.

44Solid combustible minerals

88Peat

In the studied area 36 peat deposits are studied and evaluated; peat is being used by the local inhabitants as the fuel and fertilizer. Voytivetske deposit only is in industrial production. All peat reserves in the area are estimated and resources are evaluated. There are no perspectives for discovery of new deposits. All deposits are small-scale and their raw materials are of low quality.

45Metallic mineral resources

89Rare metals

Molybdenum

The territory perspectives for molybdenum are related first of all to Malobratalivska ore-bearing field which includes three sites: Malobratalivska, its south-eastern flank, and Lysogirska. As before, most perspective and best studied remains Malobratalivska site where average molybdenum content is 0.062% (after chemical analysis) under average ore body thickness 7.2 m. Mineragenic potential of the south-eastern flank and Lysogirska site is assessed by analogy with Malobratalivska site. High molybdenum concentrations are not identified over there. To date, further geological studies in Malobratalivska ore-bearing field are not reasonable.

90Radioactive metals

Major territory perspectives are related to Zhdanivskiy and Sokolivskiy uranium occurrences, located in the exo- and endo-contacts of Khmilnytskiy leucogranite massif with associated metasomatite bodies of albitite composition. High content of valuable component, clear control by metallogenic factors and prospecting indicators allow recommendation of specialized prospecting works in Khmilnytska ore-bearing field.

91Precious metals

Identification of Zhdanivska intrusion with increased content of platinoids and definition of the platinum mineral form – sperilite, allow considering Khmilnytska MZ as perspective for prospecting of minor ultramafic intrusions with high precious metals content.

139

46Non-metallic mineral resources

92Ore-chemical raw materials

130Agro-chemical raw materials

Apatite ores

The territory perspectives are first of all related to the discovery of apatite ore deposits where Ukrainian demands are very high for. Assessment of perspectives for this mineral type is performed on the results of GM- 50 in Letychivskiy area completed in 2002. In Goloskivske ore field the minor apatite ore deposit is foreseen with technological properties that match industrial requirements and by quality do not have analogues among explored deposits in Ukraine. In the ores of Goloskivskiy occurrence average P2O5 content is 4.9% (up to 10.5%). Apatite concentrate contain 38-39% P2O5 under extraction 70.52-76.47%. In parallel plagioclase concentrate for glass industry and pyroxene-amphibole concentrates for refractory materials manufacturing can be obtained. Mining at the deposit can be conducted by open-cast method (quarry). From the overburden apatite- bearing sands can be extracted from the basal horizon and lower column parts of Obukhivska Suite (Goloskivskiy III occurrence). In the occurrence prospecting-evaluation works are recommended. In Goloskivskiy ore field and Antonivske and Rudnyanske ore-bearing field prospecting works are recommended (in the first one these works are already underway). Perspectives of occurrences related to collophane mineralization require further studies.

93Non-metallic ore raw materials

131Adsorption raw materials

Vermiculite

Major territory perspectives for vermiculite are related to Brazhynetskiy occurrence where under relatively low overburden thickness (up to 29.0 m) economic concentration of vermiculite ores are noted (average content 17.69% over thickness 4.6 m). By analogy with Brazhynetskiy occurrence, in Grytsivske ore-bearing field by geophysical parameters 7 sites are distinguished perspective for vermiculite. Confidence of geophysical criteria in prognosis for gabbro- monzonite massifs and vermiculite deposits related to their weathering crusts is very high. In the ore-bearing field prospecting works are recommended.

132Electric- and radio-technical raw materials

Graphite

Identified graphite occurrences provided the reasons to qualify the area as medium-high-perspective for discovery of graphite deposits. In Veselkivskiy ore-bearing field the least noted depth of Bereznynska sequence graphite-bearing gneisses is 50.0 m, free carbon content – 5.58%. Ore quality matches industrial requirements but due to great depth ore-bearing field is qualified as medium-perspective. In Makharynetske ore-bearing field ore depth is much less – 3-13.0 m with relevant economic concentration of valuable component (average free carbon content is 4.83%) and by these reasons it is considered as high-perspective. Confidence of geophysical criteria, specifically, electric survey, is very high under prospecting for graphite-bearing rocks.

133Facing stone and construction raw materials

It is established in the course of prospecting works [40, 41] that garnet-biotite granites of Berdychivskiy complex by their physico-mechanic and decorative properties can be used as the raw materials for decorative- facing and block stone. Considerable distribution areas, low depth and overburden thickness along the river valleys provide favorable perspectives of mapped territory for prospecting of decorative-facing stone deposits at the sites with the least tectonic modifications.

140 Precambrian crystalline rocks (granites and migmatites of Berdychivskiy complex, charnockitoids of Gayvoronskiy and Litynskiy complexes, gneisses and mafic gneisses of Dnistersko-Buzka Series) and Sarmatian limestones are suitable for diverse-class quarry-stone manufacturing. Numerous surface exposures of these rocks are noted along major rivers (South Boug, Buzhok, Ikva, Zgar) providing favorable conditions for their mining. Both crystalline rocks and limestones in all explored deposits exhibit physico-mechanic properties allowing their use in the construction and road works. The territory is completely supported by the raw materials for quarry- stone production. Limestones are widely developed in the studied territory and can be used as the raw materials for lime manufacturing. Most perspective site for prospecting in purposes of carbonate raw materials for lime roasting is the steep right bank of Vovk river where numerous outcrops of oolite-detritus, organogenic-detritus pelito-morphic limestones are observed up to 11.3 m thick. Over there, artisanal mining is being conducted for small-scale blocks which are used in construction. Construction sands are insufficient for the area. In the course of geological mapping 30 samples were analyzed of Miocene and Miocene-Pliocene sands as well as Quaternary alluvial-deluvial and terrace sands. All samples by the content of organic admixture are lighter than etalon and are conditional. By content of dust-like, clayey and mud particles (from 4.62% to 51.18%) the sands cannot be used without beneficiation for common concrete, construction liquids and silicate brick manufacturing. Thus, despite of wide development and low depth, the territory perspectives for sands are limited because of their low quality.

47Groundwaters

In the map sheet M-35-XXII in various years Pobuzka GE of “Kyivgeologia” trust and Pravoberezhna GE of SE “Pivnichgeologia” had explored a range of the fresh groundwaters for centralized water supplying of towns and town-like villages. Groundwater reserves are approved by SCMR of USSR, Ukraine and Scientific- Technical Council of “Kyivgeologia” trust. Pravoberezhna GE had conducted groundwater prospecting for water supplying of Letychiv town, Khmelnytska Oblast, but groundwater reserves obtained in these works are not approved yet. In the map sheet area prognostic groundwater resources are evaluated. Explored and approved exploitation groundwater reserves comprise 18% of prognostic resources. The contemporary water extraction constitutes 10% of the total amount of approved reserves. Thus, the territory is supported by prognostic fresh groundwater resources and exploitation reserves. In the area of Khmilnyk town the mineral radon water reserves are explored and approved for the fracturing zone of Precambrian crystalline rocks. The “Khmilnyk” resort is operating with these waters. Resort is supported by prognostic and exploitation resources of radon waters. The total extraction of mineral waters constitutes 16.6% of the sum of approved reserves. For water supplying of rural inhabitants the wells are mainly being used constructed for the first from the surface water-bearing horizons where water quality often is not appropriate. In order to upgrade water supplying quality the exploitation boreholes should be used which are available in most inhabited localities but are out of use, and also, if necessary, to drill new exploitation boreholes for water-bearing horizons developed below the first ones from the surface.

141

1211. ECOLOGICAL-GEOLOGICAL SITUATION

Ecological-geological state of the territory is assessed be means of synthesis of all available data on the suffer degree of geological environment, its contamination by harmful substances, development of dangerous natural and technogenic processes. As a result, the sketch map of ecological state of geological environment is designed (Fig. 11.1).

Fig. 11.1. Sketch map of ecological state of geological environment in map sheet M-34-XII (Starokostyantyniv).

See next page for the legend.

142

Fig. 11.1. Continued. The legend.

Levels of ecological state of geological environment: 1 – very charged; 2 – charged; 3 – moderate charged; 4 – appropriate. Technogenic objects affecting ecological state of geological environment: 5 – heating devices; 6 – a) machinery construction, b) chemical industry; c) woodworking industry; 7 – a) construction materials, b) light and c) food industry; 8 – mining industry; 9 – agriculture complex; 10 – water-scoop devices; 11 – storage, disposal and utilization of industrial and house-holding wastes (a) solid, (b) liquid; 12 – sewage filtration fields (to the right in numerator – square, km2; in denominator – sewage amount, th.m3/year); 13 – sites of sewage water drop into rivers (to the right – sewage amount, th.m3/year; to the left – ingredient-contaminator index); 14 – sewage ponds from animal farms; 15 – communication objects (petroleum pipelines); 16 – objects- contaminators: a) petroleum stores, b) gasoline stations; 17 – territory contour of industrial-urban agglomerations and areal centers. Component and geological environment contamination by toxic chemical elements (in the contour break and next to geochemical anomaly point – chemical elements-contaminators and their concentration coefficients): 18 – soils (a) planar, b) local; 19 – bottom sediments; 20 – local groundwater contamination by toxic chemical elements and compounds. Natural radioactive contaminators: 21 – mineral deposits by radioactivity degree (a) not assessed, b) safe, c) potentially dangerous; 22 – apparent boundary of groundwaters with increased content of Rn, U; Other symbols: 23 – sites defeated by the dangerous EGP (more than 50% of the square); 24 – zone of increased tectonic activity, fracturing; 25 – pseudo-formula for ecological evaluation of the state of geological environment (G – dangerous groundwater contamination level, S – moderate-dangerous level of soil contamination, E – moderate-dangerous level of EGP defeating, e – low-degree of EGP defeating); 26 – site boundaries with assessed change or contamination in specific same-level components of geological environment); 27 – boundary of karst processes development.

In the studied area a range of major towns are located (Khmelnytskiy, Khmilnyk, Starokostyantyniv, Medzhybizh, Lyubar, and others), as well as municipal units and industrial enterprises which often do not match contemporary requirements of ecological security and negatively affect geological environment. In general, this is the area with developed agricultural complex. Of the food industry (Khmelnytskiy, Khmilnyk, Zhdanivka, Bogdanivka, Starokostyantyniv, Ostropil, Stara Synyava, Letychiv, Lyubar) the sugar, oil-fat, flour-grinding, meat, butter-making, fruit and vegetable directions predominate. The enterprises of machine-building (Khmelnytskiy), electronic, chemical, mining and light industries are also known. The household and industrial landfills comprise the source of soil, surface and groundwater contamination. Major municipal landfills are located in the areas of Khmelnytskiy, Khmilnyk, Starokostyantyniv, and other towns. Industrial enterprises and agriculture raw processing units which use considerable amount of water, are located in the major inhabited localities close to the rivers providing cleaned, low-cleaned and sometimes non-cleaned drops into the water objects. Best studied is ecological-geochemical state of South Boug river in the southern part of map sheet area (in the area of GM-50). The water-municipal enterprises drop the waters into South Boug – 18900.025 th.m3/year (Khmelnytskiy, Letychiv), Ikva – 296.6 th.m3/year (Stara Synyava), Sluch – 2788 th.m3/year (Starokostyantyniv, Lyubar). For instance, in the area of Stara Synyava town on Ikva river the technogenic hydrochemical surface water anomalies are known. The major compounds contained in excess of TAC include iron, ammonia and petroleum products. Besides that, sewages are being dropped into filtration fields: Khmelnytskiy – 0.48 th.m3/year, Khmilnyk – 0.59 th.m3/year, Starokostyantyniv – 0.541 th.m3/year.

143 In the studied area three major petroleum stores, pipelines 124.4 km long, and many gasoline stations are located which by their technological properties comprise contamination sources of geological environment – aeration zone and surface waters in rivers, lakes and reservoirs. Petroleum products are the major contaminators. Their input into aeration zone is being done through technical faultiness of petroleum product reservoirs and pipelines. The surface soils, aeration zone soils and groundwaters undergo technogenic contamination. In surface and groundwaters contamination is also observed outside petroleum stores. Water reservoir on South Boug river, numerous ponds (the bigger ones are located in Buzhok, Vovk, Ikva river valleys), quarries, drainage trenches, dams, road heaps, peat operations negatively impact on geological environment. The water reservoir on Buzhok river 46.5 km2 in size is extended over 15 km. The water reservoir on South Boug river nearby Letychiv town is about 9 km2 in size and extended over 13 km; maximum width of water table nearby Letychiv town is about 3 km. Its strewed dam width nearby Shchedrova village is about 250 m, maximum height – up to 5 m. At the low flood-land sites of South Boug, Buger, Fosa, Osyra, Ikopot and other rivers the linear irrigation channels of peat operations are located. Due to groundwater stopping by the surface river and water reservoir waters the under-flooding of inhabited localities is observed (Starokostyantyniv, Lyubar). The quarries for construction materials significantly suppress the groundwater level and also cause their contamination. It is found that technogenic activities may provide radiation-dangerous situations. In the studied area 7 quarries are in production (Golovchynetskiy, Grytsivskiy, Krasnosilkivskiy, Kutyshchanskiy, Krutnivskiy, Starosynyavskiy, Rusanivskiy), of which major ones are located in the area of Golovchyntsi and Rusanivtsi villages. These occupy small squares but are deep enough. The deepest (about 50 m) is Rusanivskiy quarry with three benches. Construction and facing stone deposits in production exhibit increased radioactivity. By the degree of radioactivity and radionuclide content distribution in the rocks three groups of deposits are distinguished: safe (VED – 5-22 mcR/h, Aef. – 81-265 Bk/kg), potentially dangerous (VED – 7-64 mcR/h, Aef. – 48-708 Bk/kg), and dangerous (VED – 5-28 mcR/h, Aef. – 33-1073 Bk/kg). During exploitation of potentially dangerous and dangerous deposits the radiation dangerous conditions may appear: for personnel in the quarry – because of wind erosion and radon emanation; for inhabitants in around quarry – through dust particle expansion after blasting, wind erosion and water filtration through the dumps [38]. The negative impact on environment is being imposed by the railways (Khmelnytskiy – Starokostyantyniv, Khmilnyk – Starokostyantyniv) and motorways, State-rank first of all: Vinnytsya – Khmelnytskiy, Chudniv – Starokostyantyniv, Khmelnytskiy – Shepetivka, and others. Major elements- contaminators include lead, zinc, manganese.

48Landscape zonation

The studied territory is ascribed to the region of forest-steppe landscape-geochemical zone. The vegetation cover features are defined by agriculture lands, meadow vegetation and mixed forests. Physico-chemical migration is defined by the neutral and low-alkali values of acid-base parameter of natural waters, calcium migration class with typomorphic calcium, rarely iron in minor amounts, acid migration classes. Geochemical satellites of typomorphic calcium include strontium, radium, barium and zinc; typomorphic hydrogen – cesium, potassium and copper; typomorphic iron – manganese, cobalt, nickel, chromium and vanadium. The following classes of geochemical landscapes by geochemical parameters and groundwater types are distinguished: acid (H+), acid-calcium (H+-Ca2+), acid-gel (H+-Fe2+), calcium (Ca2+). The acid class (H+) landscapes are developed at Trebukhivske and Litynske watershed plateaus, Letychivska and Khmilnytsko-Lukashivska transitional valleys over sod-low-podzol and podzol soils. The calcium (Ca2+) and acid-calcium (H+-Ca2+) class landscapes are developed in Litynska elevated accumulative-denudation loess plain over podzol and low-humus black earths. The acid-gel (H+-Fe2+) class landscapes are developed in the water reservoirs and flood-lands of South Boug, Ikva, Fosa, Buger rivers over geled swamp, peat-swamp and peat soils. By the relief features and groundwater level the types of geochemical landscapes are distinguished – eluvial, transiluvial, eluvial-accumulative, super-aqueous, sub-aqueous. In the modern conditions both physical and geochemical structures of the landscapes underwent essential changes caused by agricultural and mining activities and urbanization.

144

49Assessment of soil and bottom sediment contamination

Technogenic soil contamination depends on their type and amount of industrial wastes, pesticides and mineral fertilizers input, as well as element mobility in various soils. In low-humus sod-podzol soils elements- contaminators are transformed into mobile compounds and move to lower layers and groundwaters. In black earth soils these elements are in passive state and available for plants. In the southern, most studied map sheet part the following background values of chemical elements are established (in mg/kg): lead – 20, zinc – 50, copper – 20, nickel – 20, phosphorus – 800, manganese – 750. The points are identified with increased content of chemical elements (in mg/kg): I-class danger (lead – 500, zinc – 500, fluorine – 560, mercury – 0.30, phosphorus – 10000); II-class danger (copper – 2000, chromium – 500); III- class danger (manganese – 10000, strontium – 2000), and also with 2 times increases background contents (barium – 1000, titanium – 1000, niobium – 32, gallium – 20, cobalt – 20, molybdenum – 4, vanadium – 120, silver – 0.5, zirconium – 800) [51]. Chemical element-contaminators provide planar and local anomalies which differ in the bulk contamination parameter (BCP) from 1 to 128 units. Planar anomalies with BCP 32-128 are noted in the areas of Ivanyntsi village (Cu, Zn, Pb, Sn), Shrubkiv village (Cu, Sn, Pb, Ni, Zn), to the south from Dyakivtsi village (Cu, Sn, Zn, Pb, Ag), and with BCP more than 128 units – to the east from Litynka village (Pb, Cu, Zn, Sn, Sb). Local anomalies related to motorways are only encountered in the area of Goloskiv, Rozsokhy, Bokhny villages. In the area of Antonivka, Grechantsi villages slight contamination by chlorine-organic pesticides is noted (0.02- 0.06 mg/kg). Low bottom sediments contamination rate in water systems is characteristic for entire map sheet area. Linear anomalies of BCP 3-10 units are noted in Mshanetska Ruda river where major element-contaminators include lead, zinc, nickel, chromium, vanadium; in Taran river – manganese; in Ikva river, higher of Stara Synyava town – chromium (BCP 3-5 units) [52]; in Luky river, section Maydan-Verbovetskiy – Yalynivka increased copper content is noted – 80-300 mg/kg, zinc – 200-800 mg/kg, nickel, manganese (BCP 10-26 units) [51]. In the bottom sediments of South Boug river, down of Bogdanivka village, the linear anomalies are noted with increased content of barium, tin, copper, zinc, silver, phosphorus (BCP 13-26 units) but their contents do not exceed TAC [51].

50Assessment of surface and groundwater contamination

The river network of the territory belongs to the basins of Prypyat (Khomora, Sluch rivers and their branches) and South Boug (Vovk, Buzhok, Ikva, Domakha, Fosa and Kudynka rivers) rivers. By chemical composition the river waters are fresh, hydrocarbonate calcium-magnesium with mineralization from 0.4-0.6 g/dm3 [50], sulphate and chloride content is low, average hardness is 8.8 mmol/dm3, and in some sites only, at low-cleaned water drops, mineralization increases, nitrates and chlorides are noted but in the standard norm limits. In the area of Stara Synyava town on Ikva river the surface water technogenic hydrochemical anomalies are distinguished. Major ingredients in exceed TAC include iron, ammonia, petroleum products. Content of the latter attains 0.46-0.49 mg/dm3 (at TAC 0.3 mg/dm3), and iron is two time higher of TAC. Groundwaters, related to sedimentary piles, are discontinuous. In the studied area protection degree of groundwaters is different. Almost unprotected are groundwaters used in household purposes. At the watershed sites the inter-bed water-bearing horizons are confined to Neogene-Paleogene sediments and fractured zone of Precambrian rocks and classified as protected, and on the slopes – as conventionally protected. Groundwaters are sulphate-hydrocarbonate calcium and sulphate-hydrocarbonate magnesium-calcium, mineralization is 0.8-1.0 mg/dm3. Increased mineralization is noted in the are of villages Shevchenka (2181 mg/dm3), Nova Synyavka (2372 mg/dm3), Stariy Ostropil (2013 mg/dm3), Semenivka (1525 mg/dm3), Vyshnopil (2424 mg/dm3), Brazhyntsi (2609 mg/dm3), Pashkivtsi (2029 mg/dm3), and others. Increased chloride content is found in the wells of Shevchenka (400.7 mg/dm3) and Ilyatka (388.3 mg/dm3) villages. In the water-scoop devices of Khmelnytskiy town, Popivtsi, Pashkivtsi, Ugly villages, the iron contamination by 0.7 mg/dm3 is noted. In the inhabited localities the groundwater contamination by nitrates – from 1 to 8 TAC (Kozhukhiv – 192 mg/dm3, Stariy Ostropil – 243 mg/dm3, Verkhnyaky – 254.9 mg/dm3, Semenivka – 274.3 mg/dm3, Brazhyntsi – 383.9 mg/dm3, and others) is noted, in some cases – higher of 10 TAC (Pashkivtsi – 449.7 mg/dm3, Emtsi – 469.6 mg/dm3, Vyshnopil mg/dm3, Ilyatka – 512 mg/dm3, Tsymbalivka – 553.5 mg/dm3). When comparing

145 water sampling results for 1967 and 2004, it should be noted that water quality used in water supplying, is essentially changed. According to 1967 data, nitrate content was measured in single units whereas in 2004 it was 45-553.5 mg/dm3. With tectonic zones mineralized waters of different composition are related. In waters from fracturing zone of Precambrian rocks in the area of Khmilnyk town and the territory in around Gologky, Sokolove, Verkhivka and other villages the following concentrations are noted: radon – 32-2500 eman, uranium – 9.8×10-3- 1.1×10-4 g/dm3, radium – 1.1×10-7-7.3×10-4 g/dm3, in the area of Stariy Ostropil village – uranium – 1.1×10-5 g/dm3. In the waters of Quaternary sediments (in wells) in the area of Ivankivtsi, Dubrovka, Brazhyntsi villages uranium is measured to 1.1×10-5 g/dm3. In the waters of Vendian sediments in the area of Khmelnytskiy town radium is noted in amounts 4.8×10-11-1.03×10-10 g/dm3.

51Assessment of EGP suffering

The territory is located at the junction of Prydniprovska and Volyno-Podilska heights which include II- order Vinnytska and Podilska morpho-structures. Most of territory is located in Vinnytska morpho-structure and Podilska height occupies just the western part of map sheet. Over there, basement surface plunges down and hypsometric level of modern surface ascends. Structure of the lower sedimentary parts in Podilska and Vinnytska morpho-structures is different. These differences are smoothed due to Sarmatian sea transgression and further Upper Miocene – Anthropogenic erosion and accumulative-denudation activity, which played important role in the modern relief development. Miocene-Pleistocene sediments include various genetic types which differ in thickness and hypsometric position. Some sites in the territory are variously eroded because of differentiated neo-tectonic motions expressed in the modern relief. In the studied territory three age-different areas are distinguished: Lyubarska accumulative- denudation low-cut height, Starokostyantynivska denudation hill-wavy high-cut height (Litynska elevated denudation loess plain, Trebukhivske watershed uplift, Letychivska and Khmilnytsko-Lukashivska transitional valleys). Lyubarska plain occupies the northern and north-eastern map sheet parts. The territory relief is plain, slightly lowered to the north. Plain surface is cut by river valleys of various shapes and sizes, swamped flood- lands and lowlands. The lowland peat swamps are developed in the river flood-lands, and at the watershed sites are locally developed in the area of Grynivtsi, Kotelyanka villages. Swamp development is caused by significant amount of atmospheric precipitates and low relief cutting. Swamp defeating rate is 11-25%. Collapsing processes related to loess sediments are most developed nearby Maliy Vyshnopil, Demkivtsi, Lyubar villages and expressed in the oval steppe saucers. The territory defeating degree by collapsing processes varies from 3 to 10%. Sluch-Teterivska accumulative-denudation low-cut height occupies the eastern part of the studied territory. The plain surface is broken by river valleys, swamped flood-lands and lowlands. Collapsing processes are related to the loess sediments and expressed in the oval steppe saucers; the territory defeating degree varies from 3 to 10%. Litynska elevated plain is extended from the north-west to south-east with gentle inclination in the east- south-eastern direction. The modern relief altitudes vary in the range 280-365 m. In the plain mainly accumulative-denudation genetic relief type is developed at the watershed sites, denudation on the slopes and erosion-accumulative fluvial type in the gully bottoms. Of the major relief forms and elements the following can be distinguished therein: sub-aerial, erosion- accumulative (gullies and gorges), denudation, gravity (slides). The gullies comprise important constituent of the modern relief. They are arranged in the dense tree- type network. The biggest ones are 10 and more kilometers long. At the upper courses they are normally V- shaped, with low cut and gradual transitions into flat watersheds. On approaches to the mouth parts they somewhere become trough-like with symmetric sodded slopes. The cutting depth increases to 10-25 m and bottom width attains first tens of meters, in places up to 100-150 m. The gullies are commonly opened to the flood-lands. Deep gullies cut water-bearing horizons and permanent water flows are developed in their bottoms. The gorges, in comparison to gullies, are locally developed (Novosilky, Vesel, Rozsokhy, Svichna, Guli villages). These are related to the steep slopes where loess rocks are observed in direct proximity to the surface. Gorge erosion is accompanied by the soil removal and stone falls. Gorge length is from some to first tens of meters. The cutting depth is from 1.0-1.5 to 5-7 m and mainly depends on loess thickness. Gravity slide forms in the studied territory are developed almost everywhere and confined to the steep gully slopes. The slides with smoothed and sodded detachment walls predominate with variously eroded bodies. The young slopes are with well expressed detachment walls up to first meters high, hilly, in places wetted body surface, somewhere with “drunk forest”. The sliding surfaces are related to Miocene and Pliocene clays.

146 Development of sliding forms (Vesele, Semaky, Bugai, Shrubkiv villages) is related to the water- bearing horizon above clay interbeds and change in the rock physical state under their wetting at steep slope. Defeating rate by planar slides is 40%. Trebukhivske watershed plateau occupies the south-western part of the territory. The basement altitudes are mainly high – 260-290 m, and cover of Pleistocene sediments is thin – 5-15 m. The northern part is bounded by the right bank of South Boug river valley. Surface altitudes are 300-380 m. The major structure-genetic relief type is denudation-accumulative with slight predomination of denudation processes, variously expressed in different sites that reflect differentiated tectonic activity. The gorge-gully system in uplift is tree-shaped. Its structure and cutting depth are similar to those described in Litynska elevated plain. The differences include less gully density and length rarely attaining 6-7 km. The steep slopes are also often complicated by minor slide forms. Letychivska transitional valley is characterized by erosion-accumulative with superimposed sub-aerial genetic relief type, occurrence of aeolian forms, as well as swamped, in places drainage-less dimples and minor saucers. The valley relief is slightly-hilly, low-cut by gully network. The gullies are normally short (up to first kilometers) with low cut and sodded slopes. Low-cut valley relief and high amount of atmospheric precipitates had played the major role in the swamp development. The upper and lower swamps are distinguished over there. These are of various shapes and sizes, somewhere drainage-less. Normally these are weakly expressed in the relief dimples with stagnant or slightly-running waters and swamp vegetation. Their development is related to the near-surface position of water-proof horizon. Lower swamps are related to the broad (up to 1.0-1.5 km) flood-lands of South Boug, Buzhok, Ikva, Buger and Fosa rivers. Defeating rate of swamping is 11-25%. Khmilnytsko-Lukashivska transitional valley is extended in the south-eastern direction. Surface altitudes are 280-310 m in the north-western part and 240-280 m – in the south-eastern one. In tectonic respect the valley is controlled by Khmilnytska tectonic zone. The major structure-genetic relief type of the valley is erosion-accumulative with superimposed sub- aerial forms. The valley surface relief is flattened, low-hilly. The gullies are short (up to 1-2 km) with low cut and mainly flat sodded slopes. Lower peat swamps are widely developed in the flood-lands of South Boug and Domakha rivers. Defeating rate of swamping is 11-25% [33]. In the south-western map sheet part, at the sites composed of Cretaceous sediments, the karst is observed expressed in the relief with minor swamped dimples. From the above description one may conclude that contemporary tectonic plane, developed over neo- tectonic stage and expressed in the modern relief, gorge-gully and river networks, is related to the weakened zones of tectonic breaks and in many respects is inherited from the older one. According to the seismic zonation, the studied territory is non-seismic. In tectonic zones the sites of increased fracturing are observed, along which vertical migration of chemical elements is possible and contamination of fracture waters in crystalline basement. The synthesis and analysis of the whole amount of data, the sites are distinguished with various degree of changes in geological environment; the state of these sites is classified as very charged, charged, moderate- charged, and appropriate. By the soil contamination degree the territory is assessed as low-broken, except the sites, where in the soils the planar anomalies with BCP 32-128 units (Ivanyntsi, Shrubkiv, Dyakivtsi village areas) and BCP more than 128 units (Litynka village). By the degree of exogenic geological processes (EGP) defeating the territory is assessed to be appropriate except some sites of slides development and river flood-land swamping. The quality of drinking water in the first from the surface water-baring horizons by chemical composition does not match State standards for drinking water by the parameters of mineralization, hardness, and nitrate content.

147

13CONCLUSIONS

In the set of geological maps and in explanatory notes all available material is summarized obtained in the course of geological, geophysical, hydrogeological and research works, updated and elaborated during extended geological studies in the scale 1:200 000 in the map sheet M-35-XXII (Starokostyantyniv), and systematized in accordance with the modern insights and current requirements in the process of preparation to publishing. Conducted works made possible adjustment of the area geology, stratigraphic and genetic subdivision of Quaternary, pre-Quaternary, pre-Mesozoic sediments and rocks of crystalline basement, tectonic structure, history of geological development of the territory and its perspectives for various types of mineral resources. 1. In the map of Quaternary sediments: - the stratigraphic-genetic subdivision of Quaternary sediments is conducted in accordance with the valid stratigraphic scheme; the age and structure of South Boug, Sluch, Ikva river terraces are adjusted; transitional water-glacial valleys are distinguished and mapped; relations of zander and loess areas are examined. - geomorphologic zonation of the territory is adjusted. 2. In the map of pre-Quaternary units: - Sarmatian sediments are divided into three sequences. Similar approach to the stratification of these sediments is applied in the map sheet “Berdychiv” and “Vinnytsya”. The issue of distinguished sequences upgrade to stratons requires further analysis for regional features of their distribution and paleontological support; - the contours of Buchatska erosion-tectonic depression are adjusted. 3. In the map of pre-Mesozoic units: - the boundary of Vendian sediments, tightly related to the basement surface, is essentially adjusted; - litho-facial features of Vendian sediments are studied. In the map sheet two column types are distinguished characteristic for Volyno-Podilskiy trough and Podilskiy uplift of Ukrainian Shield. Two litho-tectonic zones are distinguished – Khomorska and Pivdennobuzka; - subdivision of Vendian sediments, in their Volynian part first of all, is put in compliance with the valid stratigraphic scheme; - erosion-tectonic nature of the junction between Ukrainian Shield and its slope is established. 4. In the map of crystalline basement: - the complex affinity of ultra-metamorphic granitoids in the territory is defined. In Dnistersko- Buzkiy mega-block these rocks are divided into Gayvoronskiy (?), Litynskiy, Berdychivskiy complexes, and in Volynskiy mega-block – into Sheremetivskiy and Zhytomyrskiy complexes; - the boundaries, composition and metallogenic specialization in intrusive granites of Khmilnytskiy complex are adjusted; - the composition is further studied of Bukynskiy complex intrusive rocks which constitute southern part of Varvarivskiy massif and its satellites; - association of ultramafic rocks of Zhdanivskiy massif is distinguished for the first time with absolute age after preliminary data about 1850 Ma; - tectonic structure of the area is adjusted. The boundary between Volynskiy and Dnistersko-Buzkiy mega-blocks is set by Teterivska fault zone. The boundary is complicated by the displacements along Andrushivska zone. 5. The information on mineral-resource base of the territory is systematized and elaborated. Major perspectives of the area are related to apatite of Goloskivske ore field, Zhdanivskiy radioactive metal occurrence, Grytsivskiy vermiculite-bearing field, Khmilnytske deposit of radon curative waters and deposits of construction materials. 6. Hydrogeological conditions in the area are adjusted, the distribution fields of water-bearing horizons, chemical composition of the first from the surface water-bearing horizon, directions of groundwater use. 7. Assessment is made for ecological state of geological environment. The following issues require further studies: - adjustment for the north-eastern boundary of sequences distinguished in Sarmatian regio-stage, and stratigraphic relationships of the upper part of this column with the sequence of parti-colored clays;

148 - adjustment for the boundaries of Vendian column characteristic for Volyno-Podilskiy trough and Podilskiy uplift; - adjustment for the age, genesis and complex affinity of Zhdanivska association of ultramafic rocks; - subdivision of charnockitoids in the territory on the ground of their marker absolute age determinations.

149

14REFERENCES

52Published

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53Unpublished

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150 22. Geyko, V.D., Vasilenko, N.S., 1982. Report on results of deep geological mapping in the scale 1:200 000, map sheet M-35-XXIX (Vinnitsa) and group geological mapping in the scale 1:50 000 for map sheets M-35-105-A,B,C,D; -106-A,B,C,D over 1978-1982. – Kyiv. (In Russian). 23. Germanov, B.S., et al, 1988. Results of geophysical and geochemical studies aiming preparation of basis for geological mapping in the scale 1:50 000 in the map sheets M-35-91-D, -92-A,C,D (southern half), -93- C: Report of Volynskaya geophysical and prospecting-mapping groups over 1985-1988. – Kyiv. (In Russian). 24. Dovgan, R.N., 2001. Prospecting for bedrock diamond deposits in Berdychevskoe uplift, 1999- 2001. – Kyiv. (In Russian). 25. Dubovetskiy, A.T., Timoshenko, A.I., 1974. Results of complex geophysical studies in preparation of geophysical base for geological mapping in the scale 1:50 000 for map sheets M-35-80-A,C. Volynskaya geophysical group. – Kyiv. (In Russian). 26. Egorov, V.I., et al, 1959. Report on works of Shepetovskaya geophysical group in 1957-1958. – Kyiv. (In Russian). 27. Ivanov, A.S., Baysarovich, M.N., Grigoryev, V.N., 1974. Report on results of preliminary and detailed groundwater exploration for water supplying of Khmelnik town, Vinnitskaya Oblast, UkSSR. Conducted by Pobuzhskaya geological group and Kievskaya complex geophysical expedition in 1972-1974. – Kyiv. (In Russian). 28. Ivanchenko, N.I., Stomachenko, L.A., Denisyuk, M.A., 1969. Reports on works on complex geological-hydrogeological mapping in the scale 1:50 000 in the map sheets M-35-92-B, M-35-92-D (northern half) and M-35-93-A (western half), conducted in 1965-1969. – Kyiv. (In Russian). 29. Ivanchenko V.Ya., 1985. Report on deep geological mapping in the scale 1:200 000 in the territory of map sheet M-35-XXI (Khmelnitskiy) over 1981-1985. – Kyiv. (In Russian). 30. Klochkov, V.M., 1978. Report on results of works on deep geological mapping in the scale 1:200 000 conducted in the north-western part of Ukrainian Shield, map sheet M-35-XVII (Zhytomir) in 1975-1978. – Kyiv. (In Russian). 31. Klochkov, V.M., et al, 2002. The State Geological Map of Ukraine, map sheet M-36-XXXI (Pervomaysk). – Kyiv: UkrSGRI. – (In Ukrainian). 32. Klevanaya, T.V., 1988. Complex hydrogeological and engineering-geological mapping in the scale 1:50 000 in irrigation purposes. Map sheets M-35-68-C,D; M-35-80-A,B,D (a, b). Report of hydro-irrigation mapping group over 1985-1988. – Kyiv. (In Russian). 33. Kolot, E.I., 1981. Design of integral map for conditions of exogenic geological processes in the territory of UkSSR in the scale 1:500 000. – Kyiv. (In Russian). 34. Kuzmenko, V.I., Glukhova, G.N., Martynchuk, G.P., 1980. Report on preliminary groundwater exploration for water supplying of Lyubar town in Zhytomirskaya Oblast, UkSSR, in 1980 (Exploitation reserves estimated by 01.11.1980). – Kyiv. (In Russian). 35. Kulinskiy, V.V., 1993. Groundwater prospecting for household-drinking supplying of Letychiv town, Khmelnytska Oblast. – Kyiv. (In Ukrainian). 36. Lavrov, D.A., Shcherbak, N.P., 1963. Report on rare-metal prospecting in Upper Pobuzhye and Preydnistrovya areas over 1960-1963. – Kyiv. (In Russian). 37. Lavrov, D.A., 1966. Report on results of abrasive garnet prospecting in Upper Pobuzhye over 1964- 1966. – Kyiv. (In Russian). 38. Lepilin, O.M., 2003. Design of radiation safety map for construction stone deposits. – Kyiv. (In Ukrainian). 39. Melnichuk, E.V., 1986. Results of prospecting for diamond bedrock sources in the central and western parts of Ukrainian Shield. Report on works of Pravoberezhnaya GE over 1983-1986. – Kyiv. (In Russian). 40. Mnyshenko, Yu.M., 1986. Report on block stone deposit prospecting in Letichevskiy area of Khmelnitskaya Oblast in 1984-1986. – Kyiv. (In Russian). 41. Mnyshenko, Yu.M., 1976. Report on prospecting-evaluation works conducted in 1973-1976 in the stone quarries aiming study of opportunity to get block production (Rovenskaya, Zhytomitskaya, Vinnitskaya, Cherkasskaya and Kirovogradskaya oblasts of UkSSR). Kievskaya GE 1973-1976. – Kyiv. (In Russian). 42. Myznikov, D.F., Grishchenko, S.D., 1982. Report on results of detailed exploration of Khmelnikskoe mineral radon water deposit in Vinnitskaya Oblast of UkSSR in 1979-1981 (reserve estimation by 01.09.81). – Kyiv. (In Russian). 43. Nedovis, V.K., 1985. Report on groundwaters regime study and control over their protection from exhaustion and contamination in the territory of Vinnitskaya and Khmelnitskaya oblasts in 1983-1985 with summary results over 1981-1985. – Kyiv. (In Russian).

151 44. Piyar, Yu.K., Podtelok, P.P., 1974. Geological maps on the scale 1:50 000 for map sheets M-35-80- B and M-35-80-D: Report of geological group No. 1 and Volynskaya geophysical map over 1972-1974. – Kyiv. (In Russian). 45. Polivanchuk, A.L., 1960. Report on works of Volynskaya geophysical map over 1957-1959. – Kyiv. (In Russian). 46. Plokhotnichenko, D.I., 1969. Report of Korostyshevskaya group No. 49 over 1968 on specialized field preparation for deep uranium deposits prospecting. – Kyiv. (In Russian). 47. Pochtarenko, V.I., Bochay, L.V., 1971. Report on results of deep geological mapping in the scale 1:200 000. Map sheet M-35-XXII (Starokonstantinov). Geological mapping group No. 22, 1968-1971. – Kyiv. (In Russian). 48. Rachenkov, V.O., 1967. Report on results of prospecting works for brown coal in the area of Upper Pobuzhzhya over 1964-1967. – Kyiv. (In Russian). 49. Reznichenko, N.I., Beletskiy, S.S., 1968. Report on detailed exploration of groundwaters for water supplying of Khmelnitskiy town conducted in 1964-1967 (exploitation reserve estimation by 01.01.1968. – Kyiv. (In Russian). 50. Rosliy, A.G., 1990. Groundwater prospecting for water supplying of Khmelnik town in Vinnitskaya Oblast, UkSSR, over 1989-1990. – Kyiv. (In Russian). 51. Rybalt, B.M., 2002. Geological structure and mineral resources in the upper course of South Boug river. Report on group geological mapping in the scale 1:50 000 with general prospecting in the map sheets M- 35-91-D; -92-A,C,D (southern half); -93-C. – Kyiv. (In Russian). 52. Sanina, I.V., 1995. Regional assessment of technogenic charge influence over ecological parameters of geological environment of the territory of Ukraine. – Kyiv. (In Russian). 53. Sokolenko, L.V., 1979. Report on results of groundwater prospecting for water supplying of Staraya Sinyava town in Khmelnitskaya Oblast, UkSSR. – Kyiv. (In Russian). 54. Strelkova, N.E., Denisevich, A.I., Volovnik, B.Ya., 1960. Geological map of map sheet M-35-XXII (Starokonstantinov). Report of Starokonstantinovskaya group of Lvovskaya GE over 1957-1959. – Kyiv. (In Russian). 55. Teslenko, A.V., Sokolova, K.M., 1959. Report on works of air-geophysical group in 1958-1959. – Kyiv. (In Russian). 56. Ushakova, N.I., Tsymbal, P.N., 1959. Report on works of Vinnitskaya geophysical group in 1958. – Kyiv. (In Russian). 57. Falkovich, A.L., 1990. Deep geological mapping in the scale 1:50 000 over map sheets M-36-110-A (eastern half), B,C (eastern part), D: Report of geological mapping group No. 7 in 1985-1990. – Kyiv. (In Russian). 58. Yurchyshyn, A.P., 1989. Apatite prospecting in the western part of Ukrainian Shield (Middle Prydnistrovye) in 1985-1989. – Kyiv. (In Russian).

152

15ANNEXES

94Annex 1. List of deposits and occurrences indicated in the “Geological map and map of mineral resources of pre-Quaternary units” of map sheet M-35-XXII (Starokostyantyniv)

Geological- Cell index, Mineral type, object Notes Deposit exploitation state or brief economic type and number in name and its (references description of occurrence age of productive map location cited) pile

1 2 3 4 5 Metallic mineral resources Rare metals Molybdenum Malobratalivskiy Confined to metasomatically altered in occurrence, NW zone of Khmilnykskiy fault (north- outskirt of Maliy eastern branch) charnockitoids of 47, 44, I-4-13 Brataliv village grano-diorite composition of Litynskiy Metasomatic complex. Includes three sites: 14 Malobratalivska, its south-eastern flank, and Lysogirska Rozdolivskiy; 1.0 In up to 5.0 m thick alluvial Pliocene km to E from S sands gold content is 0.29 g/m3 IV-3-98 Sedimentary 170, 312 outskirt of Rozdolivka village Precious metals Gold Derevychi In Sarmatian sands (N1gp) in the quarry occurrence, o.5 km 1 gold sign is found. Mineral form – I-3-6 Placer 13 to SE from Velyki native gold Derevychi village Zhytyntsi In Sarmatian sands (N1gp) 2 gold signs occurrence, 0.25 are found. Mineral form – native gold I-3-8 Placer 13 km to S from Zhytyntsi village Ogiivtsi In Obukhivska Suite sands (P2ob) 1 occurrence, 2.1 km gold sign is found. Mineral form – II-2-8 Placer 13 to W from Ogiivtsi native gold village Karaimivka In Sarmatian sands (N1gp) 1 gold sign occurrence, 0.5 km is found. Mineral form – native gold II-2-24 Placer 13 to SE from Karaimivka village Ilyatka occurrence, In Sarmatian sands (N1gp) 1 gold sign III-3-33 0.8 km to S from is found. Mineral form – native gold Placer 51 Ilyatka village

153

1 2 3 4 5 Radioactive metals Thorium, uranium Koskiv occurrence, Related to Lower Vendian Khomorski 1.7 km to W from layers (V1hm). In the basal horizon I-1-1 Koskiv village (depth 37.5-75.5 m) identified uranium Sedimentary 16, 38 content by gamma-spectrometry analysis 0.016% Brykulya Related to Lower Vendian Khomorski occurrence, S layers (V1hm). In sandstones and I-1-3 outskirt of gravelites (depth 98-138.8 m) identified Sedimentary 16, 38 Brykulya village uranium content by gamma- spectrometry analysis 0.022% Kapustyn Related to Lower Vendian Khomorski occurrence, 0.9 km layers (V1hm). In the basal horizon I-1-4 to NW from (depth 115-124 m) identified uranium Sedimentary 16, 38 Kapustyn village content by gamma-spectrometry analysis 0.021% Grygorivka Related to Lower Vendian Khomorski occurrence, 0.9 km layers (V1hm). In the basal horizon II-1-17 to SE from (depth 56-64 m) identified uranium Sedimentary 16, 38 Grygorivka village content by gamma-spectrometry analysis 0.033%

Starosynyavskiy In pegmatoid granite (ργPR1bd) occurrence, center identified thorium content by gamma- Hydrothermal- III-3-34 of Nova Synyavka spectrometry analysis 0.113%. Related 51 village, nearby to rare-metal (monazite) mineralization metasomatic bridge point

Guli occurrence, In pegmatoid granite (ργPR1bd) 0.3 km to E from identified thorium content by gamma- Hydrothermal- III-3-35 Guli village spectrometry analysis 0.137%. Related 28, 38 to rare-metal (monazite) mineralization metasomatic point Lelitka occurrence, Confined to milonitized biotite granites. N outskirt of Identified uranium content by gamma- Hydrothermal- III-4-36 38 Krutniv village spectrometry analysis up to 0.052% metasomatic (depth 20.4-62.35 m) Khmilnyk Confined to biotite gneiss (depth 83.8- occurrence, in 119.8 m). Identified uranium content by Hydrothermal- III-4-38 38 Khmilnyk town gamma-spectrometry analysis up to metasomatic 0.04% Non-metallic mineral resources Ore-chemical raw materials Agro-chemical raw materials Apatite Pyrogivskiy In sands of Pylypchanska Suite (K2pl) occurrence, 0.5 km by chemical analysis P2O5 content is IV-2-53 to E from 3.16-6.74%. Average thickness of ore- Sedimentary 58, 51 Pyrogivtsi village bearing layer – 3.9 m, average depth – 38.2 m

154 1 2 3 4 5

Goloskivskiy I In sands of Pylypchanska Suite (K2pl) occurrence, 2.3 km by chemical analysis P2O5 content is IV-2-54 to W from 3.42-5.82%. Average thickness of ore- Sedimentary 51 Goloskiv village bearing layer – 2.5 m, average depth – 20.0 m Goloskivskiy III In sands and basal horizon of occurrence, 1.5 km Obukhivska Suite (P2ob) by chemical to SW from analysis P2O5 content is 0.49-8.42%. IV-2-54 Goloskiv village Average thickness of ore-bearing layer Sedimentary 51 outskirt, right bank – 3.5 m, average depth – 22.1 m of South Boug river Goloskivskiy II In the basal horizon of Obukhivska occurrence, 2.9 km Suite (P2ob) by chemical analysis P2O5 to SW from content is 0.69-3.87%. Average IV-2-56 Sedimentary 51 Goloskiv village, thickness of ore-bearing layer – 1.38 m, in right bank of average depth – 23.64 m South Boug river Raw materials for soil chemical improvers Limestone Sakhnovetske Out of production deposit, S outskirt II-2-21 of Sakhnivtsi Sedimentary village, right bank of Sluch river Non-metal ore raw materials Facing stone raw materials (decorative stone) Granite, charnockite Kudynske deposit, Out of production 1.1 km to NE from Ultra- III-3-57 Kudynka village, 40 metamorphogenic left bank of South Boug river Glass and porcelain-faience raw materials Primary kaoline Popivetske deposit, Out of production Ultra- IV-3-60 at SW outskirt of 40 metamorphogenic Popivtsi village Korostky Confined to granite weathering crust. occurrence, 1.2 km Kaoline is exposed in minor quarries at I-4-10 to SE from E the depth 0.7 m. Exposed thickness of Residual 44 outskirt of kaolines – 1.2 m Korostky village Maliy Brataliv Confined to granite weathering crust. occurrence, 0.7 km Kaoline is exposed in minor quarries at I-4-12 to NW from Maliy the depth 0.1 m. Exposed thickness of Residual 44 Brataliv village kaolines – 0.6 m Mshanets Confined to granite weathering crust. occurrence, at N Kaoline is exposed at the depth 6.5 m. II-3-28 outskirt of Approximate square of conditional Residual 13 Mshanets village kaolines – 1.1 km2. Thickness – 4.0 m

155

1 2 3 4 5 Construction raw materials Petrurgy and light concrete filler raw materials Claydite Gromivka Productive sequence – Sarmatian clays occurrence, in 0.5 (N1gp) 39.3 m thick. Overburden II-2-19 km to W from thickness – 4.7 m. Approximate square Sedimentary 13 Gromivka village – about 1.5 km2. Reshnivka Productive sequence – Sarmatian clays occurrence, 1.0 km (N1gp) 32.3 m thick. Overburden II-2-20 to N from thickness – 4.8 m. Approximate square Sedimentary 13 Reshnivka village – about 1.3 km2. Illyashivka Productive sequence – Sarmatian clays occurrence, 0.75 (N1gp) 34.0 m thick. Overburden II-2-25 km to W from thickness – 1.0 m. Approximate square Sedimentary 13 Illyashivka village – about 0.9 km2. Zagirne Productive sequence – Sarmatian clays occurrence, 2.0 km (N1gp) 28.0 m thick. Overburden II-3-29 to W from Zagirne thickness – 8.0 m. Approximate square Sedimentary 13 village – about 1.7 km2. Construction lime and gypsum raw materials Limestone Grytsivske deposit, Out of production 3.2 km to W from Maslov, I-1-2 Grytsiv town, right Sedimentary 1990 bank of Khomora river Vesnyanske Out of production deposit, 1.6 km to NE from Maslov, II-2-23 Sedimentary Vesnyanka village, 1990 right bank of Sluch river Trebukhovetske Out of production deposit, 1.2 km to SW from SW outskirt of Maslov, IV-2-51 Sedimentary Trebukhivtsi 1990 village, right bank of South Boug river Quarry-stone raw materials Intrusive and ultra-metamorphic rocks Felsic (granites etc.) Grytsivske deposit, Out of production 3.0 km to E from Ultra- Maslov, I-2-5 Grytsiv village, metamorphogenic 1990 right bank of Khomora river

156 1 2 3 4 5 Lyubarske deposit, Out of production 1.0 km to S from S outskirt of Ultra- Maslov, I-4-9 Korostky village, metamorphogenic 1990 right bank of Sluch river Kutyshchenske Out of production deposit, 1.8 km to SE from Ultra- Maslov, I-4-11 Kutyshche village, metamorphogenic 1990 in both banks of Verbka river Krasnosilkivske In production deposit, at S outskirt of Ultra- Maslov, II-2-22 Krasnosilka metamorphogenic 1990 village, swamped right bank of Sluch river Ostropilske Out of production deposit, 0.3 km to Ultra- Maslov, II-3-26 SE from Stariy metamorphogenic 1990 Ostropil, left bank of Sluch river Serbynivske Out of production deposit, 0.7 km to Ultra- Maslov, II-3-27 S from Serbynivka metamorphogenic 1990 village, right bank of Zhylka river Krutnivske deposit, In production 1.0 km to W from Ultra- Maslov, II-4-37 Krutniv village, metamorphogenic 1990 right bank of South Boug river Novosynyavske Out of production deposit, 1.0 km to SE from Nova Ultra- Maslov, III-4-42 Synyavka village, metamorphogenic 1990 left bank of South Boug river Golovchynetske In production deposit. 1.0 km to Ultra- Maslov, IV-2-48 NE from metamorphogenic 1990 Golovchyntsi village Trebukhivske Out of production deposit, 1.9 km to SE from Trebukhivtsi Ultra- Maslov, IV-2-49 village, at W metamorphogenic 1990 outskirt of Golovchyntsi village

157 1 2 3 4 5 Medzhybizke Out of production deposit, 1.0 km to SW from Ultra- Maslov, IV-2-50 Medzhybizh town, metamorphogenic 1990 right bank of South Boug river Rusanivske In production deposit, 0.3 km to SE from Rusanivtsi Ultra- Maslov, IV-2-52 village, right bank metamorphogenic 1990 of South Boug river Kudynske deposit, Out of production 0.3 km to N from Ultra- Maslov, IV-3-58 Kudynka village, metamorphogenic 1990 left bank of South Boug river Markivetske Out of production deposit, 0.3 km to NW from Ultra- Maslov, IV-3-61 Markivtsi village, metamorphogenic 1990 left bank of South Boug river Carbonate rocks Limestone Stavnytske deposit, Out of production 1.0-1.5 km to NW from Stavnytsya Maslov, IV-2-46 Sedimentary village, terrace of 1990 South Boug river left bank Golovchynetske Out of production deposit, at N outskirt of Maslov, IV-2-47 Golovchyntsi Sedimentary 1990 village, terrace of South Boug river left bank Antonivske Periodically in production since 1998 deposit, 0.8 km to NW from NW outskirt of Maslov, IV-3-59 Sedimentary Antonivka village, 1990 terrace of South Boug river right bank Terlivske deposit, Out of production at NW outskirt of Maslov, IV-3-63 Terlivka village, Sedimentary 1990 terrace of Vovk river right bank

158

1 2 3 4 5 Waters Groundwaters Mineral waters Radon Khmilnytske In exploitation Pogoni- III-4-39 deposit, Fractured na, 1993 Ugrynivska site Khmilnytske In exploitation deposit, Kurortna Gayun, III-4-40 Fractured site, Khmilnyk 1962 town Fresh Lyubarske deposit, Out of exploitation Markivska site, to I-3-7 S from Lyubar Fractured 34 town, Sluch river valley Starokostyantynivs In exploitation ke deposit, Pashkivetska site, Zharin, II-1-14 5 km to SE from Fractured 1970 Starokostyantyniv town, left bank of Ikopot river Starokostyantynivs In exploitation ke deposit, KECH site, in Zharin, II-1-15 Fractured Starokostyantyniv 1970 town, Ikopot river valley Starokostyantynivs In exploitation ke deposit, Grygorivska site, 6 Zharin, II-1-16 km to W from Fractured 1970 Starokostyantyniv town, Sluch river valley Pashutynske Out of exploitation deposit, Pashutynska site, Steblev- III-1-30 15 km to S from Fractured skiy, Khmelnytskiy 1976 town, Buzhok river valley Starosynyavske Out of exploitation deposit, Mysyurivska site, III-3-31 S outskirt of Stara Fractured 53 Synyavka village, Khrystosivka river valley Starosynyavske In exploitation III-3-32 Fractured 53 deposit, KKP site

159 1 2 3 4 5 Khmilnytske Out of exploitation III-4-41 deposit, Fractured 27 Sydorivska site Khmelnytske Out of exploitation deposit, Tsentralna Steblev- site, in IV-1-43 Fractured skiy, Khmelnytskiy 1976 town, South Boug river valley Khmelnytske Out of exploitation deposit, Kudrynska Steblev- IV-1-44 site, in Fractured skiy, Khmelnytskiy 1976 town Khmelnytske Out of exploitation deposit, Pyrogivska site, 10 Gnatyuk, IV-1-45 Fractured km to E from 1971 Khmelnytskiy town Letychivske Out of exploitation IV-3-62 deposit, in Fractured 35 Letychiv town

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95Annex 2. List of deposits and occurrences indicated in the “Geological map and map of mineral resources of Quaternary sediments” of map sheet M-35-XXII (Starokostyantyniv)

Geological- Cell index, Notes Mineral type, object name Deposit exploitation state or brief economic type and number in (references and its location description of occurrence age of productive map cited) pile

1 2 3 4 5 Combustible mineral resources Solid combustible mineral resources Peat Grytsivske deposit, to S Out of production from Verbytsi, I-1-64 Korpylivka villages, to Sedimentary 12 N, SE and SW from Mykulyn village Mukhovetske deposit, 15 Out of production km to SW from Grytsiv I-1-66 Sedimentary 12 town, to NW from Brykulya village Penky deposit, 0.5 km to Out of production I-1-67 Sedimentary 12 SE from Penky village Yurovshchyna deposit, to Out of production I-2-68 SW from Yurovshchyna Sedimentary 12 village Onatskivtsi deposit, to E Out of production I-2-69 Sedimentary 12 from Onatskivtsi village Kustivtsi deposit, to SE Out of production I-2-71 Sedimentary 12 from Kustivtsi village Vorobiivka deposit, 1.5 Out of production I-2-72 km to W from Sedimentary 12 Vorobiivka Matsevychi deposit, in Out of production I-2-73 Sedimentary 12 Mal. Matsevychi village Chorna deposit, Chorna Out of production I-2-75 Sedimentary 12 village Bilkovynske deposit, to S Out of production I-2-76 Sedimentary 12 from Khyzhnyky village Rudyanske deposit, to Out of production I-3-77 SW from Mala Sedimentary 12 Derevychka village Osyrske deposit, 0.5 km Out of production I-3-80 Sedimentary 12 to SW from Lyubar town Severynske deposit, to Out of production I-3-81 NE from Severyny Sedimentary 12 village Martynivka deposit, to Out of production I-3-82 SW from Martynivka Sedimentary 12 village Bratalivske deposit, in Out of production I-4-83 Sedimentary 12 Velykiy Brataliv village

161 1 2 3 4 5 Maliy Chernyatyn Out of production deposit, 0.5 km to SE II-1-85 Sedimentary 12 from Maliy Chernyatyn village Bilkivske deposit, to SE Out of production I-2-87 from Irshynky village, to Sedimentary 12 NW from Rayky village Lazheva deposit, 1.0 km Out of production II-2-90 to E from Lazheva Sedimentary 12 village Penivske deposit, to SE Out of production II-3-94 Sedimentary 12 from Ozharivka village Koranske-I, 11 km to SE Out of production II-4-96 Sedimentary 12 from Lyubar town Snivodivske deposit Comprises some separated sites. Of these, in map sheet M-35- XXII is located site to N from II-4-98 Torchyn village, to S from Sedimentary 12 Skarzhyntsi village. Out of production Buzhokske deposit Comprises some separated sites. Of these, in map sheet M-35- III-1-100 XXII is located site to S from III-1-104 Pashutyntsi village, to NW from Sedimentary 12 IV-2-120 Medzhybizh village. Out of production Shpychynivske deposit, Out of production to SE from Paplyntsi III-3-105 Sedimentary 12 village, to NW from Podolyany village Synyavske deposit, in 5 Out of production III-3-107 km to NE from Stara Sedimentary 12 Synyava village Voytivetske deposit Comprises some separated sites. III-4-111 In production Vovkivske deposit, site Out of production in 0.5 km to S from IV-3-118 Sedimentary 12 Lugove village, to S from Shumivtsi village Golovchyntsi deposit, to Out of production IV-2-123 E from Medzhybizh Sedimentary 12 village Vovkivske deposit, site Out of production to NE from Nyzhne IV-3-128 Sedimentary 12 village, to SW from Rudnya village Tarnavske deposit, 1.5 Out of production IV-3-129 km to N from Sedimentary 12 Grushkivtsi village Kusykivske deposit, Out of production IV-4-131 Sedimentary 12 Kusykivtsi village

162 1 2 3 4 5 Kulygske deposit, site to Partly is located in map sheet M- E from Litynka village, 35-XXII. IV-4-132 Sedimentary 12 Bugar river valley Out of production Metallic mineral resources Precious metals Gold Borushkivtsi occurrence, In modern alluvium sands S outskirt of Borushkivtsi (visible thickness 1.5 m) by I-3-79 village mineralogical analysis 2 signs of Placer 13 gold are identified. Mineral form – native gold Gubyn occurrence, 2.1 In modern alluvium sand pan km to NE from Gubyn sample 1 sign of gold is II-2-88 village, Sluch river identified. Mineral form – native Placer 13 course gold Makharyntsi occurrence, In modern alluvium sand pan 1.5 km to SE from sample 1 sign of gold is II-3-91 Makharyntsi village, identified. Mineral form – native Placer 13 Popivka river course gold Non-metallic mineral resources Construction raw materials Brick-tile raw materials Loam Grytsivske deposit, W Out of production Maslov, I-1-65 Sedimentary outskirt of Grytsiv town 1990 Moskvytyanivske Out of production Maslov, I-2-70 deposit, NW outskirt of Sedimentary 1990 Moskvytyanivka village Velykomatsevytske Out of production deposit, 1.5 km to NE Maslov, I-2-74 Sedimentary from Velyki Matsevychi 1990 village Kipchyvetske deposit, Out of production Maslov, I-3-78 NW outskirt of Sedimentary 1990 Kipchyntsi village Popivetske deposit, SE Out of production Maslov, II-1-84 outskirt of Popivtsi Sedimentary 1990 village Starokostyantynivske Out of production deposit, 150 m to W from Maslov, II-1-86 Sedimentary Starokostyantyniv- 1990 Shepetivka motorway Sakhnovetske deposit, W In production Maslov, II-2-89 outskirt of Krasnosilka Sedimentary 1990 village Ostropilske deposit, to Out of production Maslov, II-3-92 Sedimentary NW from Ostropil village 1990 Levkivske deposit, 0.4 Out of production Maslov, II-3-93 km to NE from Levkivka Sedimentary 1990 village Berezivske deposit, N Out of production Maslov, II-4-97 outskirt of Berezivka Sedimentary 1990 village

163 1 2 3 4 5 Kruchanske deposit, 0.3 Out of production Maslov, III-1-99 km to E from Sedimentary 1990 Myrolyubne village Pashkivetske deposit, 2.0 Out of production Maslov, III-1-101 km to E from Pashkivtsi Sedimentary 1990 village Kantivske deposit, N Out of production Maslov, III-2-102 outskirt of Kantivka Sedimentary 1990 village Starosynyavske deposit, Out of production Maslov, III-3-106 NE outskirt of Stara Sedimentary 1990 Synyava village Krasnosilkivske deposit, Out of production Maslov, III-3-108 0.3 km to N from Sedimentary 1990 Krasnosilka village Zalisyanske deposit, 0.5 Out of production Maslov, III-4-109 km to W from Zalissya Sedimentary 1990 village Zhdanivske deposit, 5.0 Out of production km to NW from Maslov, III-4-110 Sedimentary Zhmilnyk town, nearby 1990 Zhdanivka village Malo Mytnytske deposit, Out of production Maslov, III-4-112 S outskirt of Maliy Sedimentary 1990 Mytnyk village Khmilnytske deposit, NE Out of production Maslov, III-4-113 outskirt of Khmilnyk Sedimentary 1990 town Khmilnytske II deposit, Out of production Maslov, III-4-114 NE outskirt of Khmilnyk Sedimentary 1990 town Medzhybizke deposit, 2.5 Out of production Maslov, IV-2-121 km to NW from Sedimentary 1990 Medzhybizh village Parkhomivetske deposit, In production Maslov, IV-2-122 SE outskirt of Sedimentary 1990 Parkhomivtsi village Novokostyantynivske Out of production Maslov, IV-3-124 deposit, E outskirt of Sedimentary 1990 Novokostyantyniv village Shchedrivske deposit, in Out of production Letychiv town, nearby Maslov, IV-3-125 Sedimentary dam of Shchedrivska 1990 power station Letychivske deposit, 3.5 Out of production km to NW from Letychiv Maslov, IV-3-127 Sedimentary town, right bank of South 1990 Boug river Kozhukhivske deposit, E Out of production Maslov, IV-4-130 outskirt of Kozhukhiv Sedimentary 1990 vollage Yablunivske deposit, 1.2 Out of production Maslov, IV-4-133 km to NW from Sedimentary 1990 Yablunivka village

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96Annex 3. List of deposits and occurrences indicated in the “Geological map and map of mineral resources of crystalline basement” of map sheet M-35-XXII (Starokostyantyniv)

1 2 3 4 5 Metallic mineral resources Non-ferrous and base metals Nickel Zhdanivka Related to Zhdanivskiy mafic-ultrmafic occurrence, 0.2 km massif ~350×150 m in size, with to SE from defined vertical thickness 170 m. Zhdanivka village Nickel content in nontronite weathering crust, serpentinites and low-altered pyroxenites and peridotites attains III-4- 0.524-1.617% at the depth 87.0-93.0 m. Hydrothermal- 24 149a Content after numeric analysis: Co – up metasomatic to 0.08%, Cu – up to 0.52%, Cr – up to 0.408%. Content of platinoids at the depth 85.0-93.0 m: Pt – 0.11 g/t, Pd – 1.2 g/t, Ru – 1.09 g/t, and Au – up to 0.36 g/t. Silver content at the depth 105.0-109.0 m attains 17-22 g/t Titanium Rusanivtsi Confined to gneiss weathering crust. occurrence, 0.5 km Thickness of productive ore interval – Hydrothermal- IV-2-155 to NE from 6.0 m, overburden – 9.0 m. After 51 Rusanivtsi village mineralogical analysis (depth 9.0-15.0 metasomatic m) ilmenite content – 4.22 kg/m3. Suslivtsi Confined to charnockite and enderbite occurrence, 1.6 km weathering crust, extended in sub- to NE from longitudinal direction over 360 m. Hydrothermal- IV-3-162 Suslivtsi village Overburden rock thickness – 17.18 m, 51 ore body – 3.0 and 7.5 m. After metasomatic mineralogical analysis ilmenite content – 52.3 and 61.6 kg/m3. Verbky Confined to quartz syenite gruss occurrence, 2.1-2.6 weathering crust. Thickness of km to NW from productive ore interval – 5.0 and 6.5 m, Hydrothermal- IV-3-165 Verbka village overburden – 29.0 and 44.0 m. After 51 mineralogical analysis (depth 29.0-34.0 metasomatic and 44-50.5 m) ilmenite content – 36.3 and 61.6 kg/m3, zircon – 3.74 kg/m3.

165

1 2 3 4 5 Rare metals Molybdenum Kovalenkivskiy Confined to coarse-medium-grained occurrence, to SE granodiorites. After spectral analysis from Kovalenky molybdenum content - 0.011-0.1% village (depth 50.0-160.0 m), 0.057-0.19% (depth 106.5-107.3 m). Concomitant Hydrothermal- I-4-142 elements: Sb – 0.015%, Sn – 0.005%, 44, 14 Ba – 0.2-0.5%, P – 0.2-0.5%, Cu – metasomatic 0.002-0.1%. Slight microclinization and amphibolization are observed. Length of potentially ore zone by periphery – about 8 km Rare-earth metals Monazite Rozhny Confined to vinnytsite gruss weathering occurrence, 1.2 km crust. Thickness of productive ore to NW from interval – 8.0 m, overburden rocks – Hydrothermal- III-3-148 51 Rozhny village 54.0 m. After mineralogical analysis metasomatic (depth 54.0-62.0 m) monazite content – 2.2 kg/m3. Dibrovka Confined to weathering crust of occurrence, to NW cataclased granites. After mineralogical Hydrothermal- III-4-150 28 from Dibrovka analysis (depth 66.8-71.8 m) monazite metasomatic village content – 11.1 kg/m3. Shrubkiv Confined to garnet-biotite granite gruss occurrence, 0.95 weathering crust. Thickness of km to S from productive ore interval – 8.0 m, Hydrothermal- IV-2-154 51 Shrubkiv village overburden rocks – 33.0 m. After metasomatic mineralogical analysis (depth 33.0-41.0 m) monazite content – 2.2 kg/m3. Suslivtsi Confined to pyroxene syenite gruss occurrence, 2.5 km weathering crust. Thickness of to NE from productive ore interval – 2.0 m, Hydrothermal- IV-3-159 51 Suslivtsi village overburden rocks – 14.5 m. After metasomatic mineralogical analysis (depth 14.5-16.5 m) monazite content – 7.26 kg/m3. Shchedrova Confined to garnet-biotite granite occurrence, 2.2 km weathering crust. After mineralogical 3 Hydrothermal- IV-3-160 to NW from analysis monazite content – 2.2 kg/m 51 Shchedrova village (depth 46-50 m) and 2.64 kg/m3 (depth metasomatic 33.0-38.0 m) Markivtsi Confined to feldspar-quartz fine- occurrence, 0.5 km medium-grained sand. Thickness of to S from productive ore interval – 3.0 m, Hydrothermal- IV-3-163 51 Markivtsi village overburden rocks – 0.5 m. After metasomatic mineralogical analysis (depth 0.5-3.5 m) monazite content – 5.08 kg/m3.

166 1 2 3 4 5 Verby occurrence, Confined to garnet-biotite granite. 3.0 km to NW Thickness of productive ore interval – Hydrothermal- IV-3-164 from Verbka 5.0 m, overburden rocks – 15.0 m. 51 village After mineralogical analysis (depth 15- metasomatic 20 m) monazite content – 5.08 kg/m3. Bokhny Confined to pegmatoid granite. occurrence, 2.5 km Thickness of productive ore interval – to W from Bokhny 6.3 m, overburden rocks – 46.0 m. village After mineralogical analysis (depth Hydrothermal- IV-3-167 51 46.0-52.3 m) monazite content – 3.12 metasomatic kg/m3.

Radioactive metals Thorium, uranium Veselka Confined to leucocratic medium- occurrence, E coarse-grained granites. After gamma- Hydrothermal- I-4-139 38 outskirt of Veselka spectrometry, thorium content – 0.06% metasomatic village (depth 225.3-225.6 m) Zhdanivka Confined to exo-contact of ultramafic occurrence, E massif with granitoids of Berdychivskiy outskirt of complex, directly related to albite Zhdanivka village metasomatites. After X-ray-spectral analysis, radioactive element content Hydrothermal- III-4-149 24, 38 (depth 76.15-79.0 m): uranium – metasomatic 0.0733-0.0893%, thorium – 0.0098- 0.0126%; fater gamma-spectrometry (depth 118.4-120.3 m): uranium – 0.0072%, thorium – 0.0133% Sokolova In 4 km from Zhdanivskiy occurrence. occurrence, 1.0 km After gamma-spectrometry uranium Hydrothermal- III-4-151 38 to NW from content – up to 0.042% (depth 23.0- metasomatic Sokolova village 123.3 m) Goloskiv Confined to contact of enderbites and occurrence, 1.6 km skarns. After gamma-spectrometry Hydrothermal- IV-2-156 38 to W from thorium content – up to 0.058% (depth metasomatic Goloskiv village 59.4-66.75 m) Suslivtsi Confined to pegmatoid granite. After occurrence, 1.3 km gamma-spectrometry thorium content – Hydrothermal- IV-3-158 38 to E from Suslivtsi up to 0.038% (depth 29.4-34.0 m) metasomatic village Bokhny Confined to cataclasite after garnet- occurrence, 2.5 km biotite migmatite. After gamma- Hydrothermal- IV-3-167 38 to W from Bokhny spectrometry thorium content – up to metasomatic village 0.079% (depth 46.7-57.0 m) Lelitka occurrence, Confined to garnet-biotite granite. After Hydrothermal- IV-4-168 1.2 km to E from gamma-spectrometry uranium content – 38 Stara Guta village up to 0.019% (depth 15.0-51.1 m) metasomatic Dyakivtsi Confined to cataclasite after garnet- occurrence, SE biotite migmatite. After gamma- Hydrothermal- IV-4-169 38 outskirt of spectrometry thorium content – up to metasomatic Dyakivtsi village 0.056% (depth 75.3-76.0 m)

167 1 2 3 4 5 Non-metallic mineral resources Ore-chemical raw materials Agro-chemical raw materials Apatite Goloskivskiy Confined to gabbroids and their occurrence, 2.0 km weathering crust. After chemical to S from Goloskiv analysis, average P2O5 content – 4.9%. village Prognostic square of ore body (massif) 58, 23, IV-2-157 2 Metasomatic – 0.34 km , vertical range of 51 mineralization – 150 m. Average ore volume weight – 2.97 t/m3. Ore-bearing coefficient – 0.8 Verbkivskiy Confined to alkaline rock massif occurrence, 3.6 km (shonkinites, pyroxene-biotite syenites, IV-3-166 to NW from pyroxenites). After chemical analysis, Metasomatic 51 Verbka village P2O5 content varies from 1.6 to 4.5%. Non-metallic ore raw materials Electric- and radio-technical raw materials Graphite Pedynka Confined to graphite-biotite gneisses, occurrence, 0.75 garnet-biotite granites and graphite- km to SW from hydromica-kaolinite weathering crust. Pedynka village By geophysical data, ore zone length I-3-136 attain 7.0 km, thickness – 150 m, depth Metamorphogenic 13 – 20.0-30.0 m. Total productive square – about 1 km2. Free carbon content in occurrence varies from 0.59-1.11 to 3.33-5.94% Lypne occurrence, Confined to garnet-graphite-biotite 2.3 km to W from gneisses. After chemical analysis Lypne village (depth 58.0-61.7 m) free carbon content (CC) – 5.49%, analytical moisture (WA) I-4-137 – 0.8%, ash content AC – 87.5%, Metamorphogenic 44, 15 C carbonate index (CO2) – 0.11%. In the same interval after spectral analysis content of Cu – 0.02%, Sc – 0.005% Veselka 1 Confined to graphite-biotite gneisses. occurrence, 1.85 After chemical analysis (depth 50.0- km to N from 58.0 m) free carbon content (CC) – Veselka village 5.54%, analytical moisture (WA) – I-4-138 0.8%, ash content AC – 89.6%, Metamorphogenic 44, 15 C carbonate index (CO2) – no. In the same interval after spectral analysis content of Cu – 0.05%

168 1 2 3 4 5 Veselka 2 Confined to graphite-biotite gneisses. occurrence, 0.95 After chemical analysis (depth 38.0- km to W from 49.0 m) free carbon content (CC) – Veselka village 2.52%, analytical moisture (WA) – 0.4%, ash content AC – 94.3%, C carbonate index (CO2) – 0.77%. In the I-4-141 same interval after spectral analysis Metamorphogenic 44, 15 content of Cu – 0.02-0.05%. In gneiss weathering crust (depth 22.4-30.0 m) free carbon content (CC) – 1.63-2.43%, analytical moisture (WA) – 0.8-0.9%, ash content AC – 91.2-91.5%, carbonate C index (CO2) – 0.44%. Makharynetskiy Confined to graphite-biotite gneisses. occurrence, 0.5 km Ore body comprises complex bed to SE from WNW by strike, dipping to NNW Makharyntsi under 45o. Thickness of graphite body – village 160-50 m, length – about 1.8 km, total II-3-144 square – 0.66 km2, depth from surface – Metamorphogenic 13 3.0-13.0 m (studied to depth 210 m). Average free carbon content in occurrence – 4.83%. Volume weight of graphite ore – from 2.23 to 2.6 g/cm3. Mshanets Confined to graphite-biotite gneisses occurrence, 2.0 km and garnet-biotite granites. By to W from geophysical data, ore zone length – 5.0 II-3-146 Mshanets village km, thickness – 200 m, depth – 70-100 Metamorphogenic 13 m. Possible productive square – about 2 km2. Free carbon content in occurrence varies from 0.57 to 4.35% Paplyntsi Confined to garnet-graphite-biotite occurrence, 1.0 km gneisses. After chemical analysis to SE from (depth 41.9-42.8 m) free carbon content III-3-147 kolkhoz yard in (CC) – 3.7%, analytical moisture (WA) Metamorphogenic 47 C Paplyntsi village – 0.08%, carbonate index (CO2) – 0.7%. Adsorption raw materials Vermiculite Brazhynetskiy Confined to hydromica weathering occurrence, 2.7 km crust of Brazhynetskiy gabbro- to SE from monzonite massif, identified by Residual in I-3-135 Brazhyntsi village geophysical surveys. Thickness of 13 vermiculite-bearing weathering crust – weathering crusts 6.1 m, overburden – 25.7 m. Occurrence square – 2.54 km2. Glass and porcelain-faience raw materials Primary kaoline Velyki Derevychi Confined to leucocratic granite occurrence, to NE weathering crust. Kaoline is exposed at I-3-134 from Velyki the depth 12-20 m. Approximate square Residual 13 Derevychi village of conditional kaolines – 2.1 km2. Thickness – 6.0-8.0 m

169 1 2 3 4 5 Avratyn Confined to granite weathering crust, occurrence, NE exposed in minor quarries at the depth I-4-143 Residual 44 outskirt of Avratyn 0.6 m. Exposed thickness – 0.5 m village Rogizna, area of Confined to granite weathering crust. Ozharivka and Kaoline is exposed at the depth 10.7- II-3-145 Rogizna villages 19.0 m. Approximate square of Residual 13 conditional kaolines – 5.7 km2. Thickness – 2.2-13.5 m Waters Groundwaters Mineral waters Radon Khmilnytske In exploitation Gayun, III-4-153 Fractured deposit, Lisna site 1962 Khmilnytske Out of exploitation deposit, Golodkynska site, 0.5 km to W from 27, Golodky village, III-4-159 Fractured Kostarev, 2.7-4.9 km to SE 1972 from Khmilnyk town, right bank slope of South Boug river valley Fresh Popivetske deposit, Out of exploitation 27, site of animal farm IV-3-161 Fractured Kostarev, complex of 1972 Popivtsi village

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V.V.Lukash, E.V.Gadyuchka, O.G.Lisnyak, G.G.Vynogradov. K.M.Perelygin, Z.P.Okhynko, N.K.Grytsenko, L.V.Bedrak, A.V.Fedorov

STATE GEOLOGICAL MAP OF UKRAINE

Scale 1:200 000

Central-Ukrainian Series Map Sheet: M-35-XXII (Starokostyantyniv)

EXPLANATORY NOTES

Editor Z.P.Okhynko Computer arrangement A.V.Koltsova Technical Editor A.V.Koltsova

English translation and computer arrangement B.I.Malyuk (2010)

Published according to the decision of Scientific-Editorial Council of the State Geological Survey of the Ministry of Environment Protection of Ukraine on February 15, 2007 (Protocol No. 180)

Published by SE “Pivnichgeologia”.

Address: 02088, Kyiv, Geophysicist Lane, 10 Tel.: 564-87-26; tel./fax: 564-84-62 E-mail: [email protected]

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