Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga)
The U-Pb age of zircon populations from metadacite of the Huliaipole Suite was determined using the LA-ICP-MS method as 3085-2850 and 3700-3360 Ma. In addition, two crystals of zircon were discovered with an age of more than 3800 Ma. According to geological and geochronological data, the Huliaipol...
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Видавничий дім "Академперіодика" НАН України
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| Цитувати: | Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) / G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker // Доповіді Національної академії наук України. — 2020. — № 12. — С. 48-59. — Бібліогр.: 18 назв. — англ. |
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irk-123456789-1742722021-01-12T01:26:09Z Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) Artemenko, G.V. Shumlyanskyy, L.V. Wilde, S.A. Whitehouse, M.J. Bekker, A.Yu. Науки про Землю The U-Pb age of zircon populations from metadacite of the Huliaipole Suite was determined using the LA-ICP-MS method as 3085-2850 and 3700-3360 Ma. In addition, two crystals of zircon were discovered with an age of more than 3800 Ma. According to geological and geochronological data, the Huliaipole Block, 30 × 50 km in size, is composed of rocks and relicts of the Hadean, Archean, and Palaeoproterozoic eons. The oldest nucleus of the Azov Domain was probably formed from 3.97 to 3.3 Ga ago. In the Mesoarchean (3.2-3.0 Ga), it became a part of the Middle Dnieper-Azov-Kursk granite-greenstone terrane. Felsic and intermediate volcanics of the Huliaipole Suite could have formed due to the melting of the sialic crust, including rocks of the Hadean and Archean age, as a result of the underplating of basic melts during the formation of the Neoarchean to Paleoproterozoic rift structures. Методом LА-ICP-MS визначено U-Pb вік популяцій циркону з метадацитів гуляйпільської світи — 3085— 2850 і 3700—3360 млн років. Крім того, виявлено два кристали циркону віком понад 3800 млн років. Згідно з геологічними і геохронологічними даними, Гуляйпільський блок, який має розміри 30 × 50 км, складений породами і їх реліктами гадейського, архейського і палеопротерозойського еонів. Найдавнішим фундаментом Приазовського мегаблока є, ймовірно, породи нуклеарної структури, яка формувалася від 3,97 до 3,3 млрд років. У мезоархеї (3,2—3,0 млрд років) вона стала частиною Середньопридніпровсько-Приазовсько-Курського граніт-зеленокам'яного терейну. Вулканіти кислого і середнього складу гуляйпільської світи могли утворитися внаслідок плавлення порід сіалічної кори, що включала породи гадейського і архейського віку, в результаті андерплейтингу базитових розплавів під час формування неоархей-палеопротерозойських рифтогенних структур. 2020 Article Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) / G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker // Доповіді Національної академії наук України. — 2020. — № 12. — С. 48-59. — Бібліогр.: 18 назв. — англ. 1025-6415 DOI: doi.org/10.15407/dopovidi2020.12.048 http://dspace.nbuv.gov.ua/handle/123456789/174272 550.4 (477); 551.21:551.24 en Доповіді НАН України Видавничий дім "Академперіодика" НАН України |
| institution |
Digital Library of Periodicals of National Academy of Sciences of Ukraine |
| collection |
DSpace DC |
| language |
English |
| topic |
Науки про Землю Науки про Землю |
| spellingShingle |
Науки про Землю Науки про Землю Artemenko, G.V. Shumlyanskyy, L.V. Wilde, S.A. Whitehouse, M.J. Bekker, A.Yu. Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) Доповіді НАН України |
| description |
The U-Pb age of zircon populations from metadacite of the Huliaipole Suite was determined using the LA-ICP-MS
method as 3085-2850 and 3700-3360 Ma. In addition, two crystals of zircon were discovered with an age of more
than 3800 Ma. According to geological and geochronological data, the Huliaipole Block, 30 × 50 km in size, is composed
of rocks and relicts of the Hadean, Archean, and Palaeoproterozoic eons. The oldest nucleus of the Azov Domain
was probably formed from 3.97 to 3.3 Ga ago. In the Mesoarchean (3.2-3.0 Ga), it became a part of the Middle
Dnieper-Azov-Kursk granite-greenstone terrane. Felsic and intermediate volcanics of the Huliaipole Suite could
have formed due to the melting of the sialic crust, including rocks of the Hadean and Archean age, as a result of the
underplating of basic melts during the formation of the Neoarchean to Paleoproterozoic rift structures. |
| format |
Article |
| author |
Artemenko, G.V. Shumlyanskyy, L.V. Wilde, S.A. Whitehouse, M.J. Bekker, A.Yu. |
| author_facet |
Artemenko, G.V. Shumlyanskyy, L.V. Wilde, S.A. Whitehouse, M.J. Bekker, A.Yu. |
| author_sort |
Artemenko, G.V. |
| title |
Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) |
| title_short |
Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) |
| title_full |
Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) |
| title_fullStr |
Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) |
| title_full_unstemmed |
Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) |
| title_sort |
stages in evolution of earth's crust recorded by the huliaipole block of the west azov area (4.0-2.0 ga) |
| publisher |
Видавничий дім "Академперіодика" НАН України |
| publishDate |
2020 |
| topic_facet |
Науки про Землю |
| url |
http://dspace.nbuv.gov.ua/handle/123456789/174272 |
| citation_txt |
Stages in evolution of Earth's crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga) / G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker // Доповіді Національної академії наук України. — 2020. — № 12. — С. 48-59. — Бібліогр.: 18 назв. — англ. |
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Доповіді НАН України |
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48 ISSN 1025-6415. Dopov. Nac. akad. nauk Ukr. 2020. № 12: 48—59
Ц и т у в а н н я: Artemenko G.V., Shumlyanskyy L.V., Wilde S.A., Whitehouse M.J., Bekker A.Yu. Stages in
evolution of Earth’s crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga). Допов. Нац.
акад. наук Укр. 2020. № 12. С. 48—59. https://doi.org/10.15407/dopovidi2020.12.048
Introduction. In the Ukrainian Shield, rocks of the Earth’s early crust were found in the Azov
and Dniester-Bouh regions [1-3]. In the Dniester-Bouh region, they are highly metamorphosed
and represented by enderbites and mafic crystalline schists with an age up to 3.8 Ga. A special
feature of the Azov Domain is a relatively weak metamorphism of Archean rocks, not exceeding
the epidote-amphibolite and amphibolite facies. Here, tonalites with ages of 3.67, 3.5, and 3.3 Ga
have been identified. Metaterrigenous rocks in the Soroki greenstone structure (GS) and Neo-
archean to Palaeoproterozoic troughs contain detrital zircon of Paleoarchean and Eoarchean ages
from 3.3 to 3.8 Ga [4], which indicate the presence of yet undiscovered ancient rocks in the
https://doi.org/10.15407/dopovidi2020.12.048
UDK 550.4 (477); 551.21:551.24
G.V. Artemenko 1, L.V. Shumlyanskyy 1, 2,
S.A. Wilde 2, M.J. Whitehouse 3, A.Yu. Bekker 4
1 M.P. Semenenko Institute of Geochemistry,
Mineralogy and Ore Formation of the NAS of Ukraine, Kyiv
2 Curtin University, School of Earth and Planetary Sciences, Perth, Australia
3 Swedish Museum of Natural History, Stockholm, Sweden
4 Department of Earth and Planetary Sciences, University of California, Riverside, USA
E-mail: regulgeo@gmail.com, leonid.shumlyanskyy@curtin.edu.au,
S.Wilde@curtin.edu.au, martin.whitehouse@nrm.se, andreyb@ucr.edu
Stages in evolution of Earth’s crust
recorded by the Huliaipole block
of the West Azov area (4.0-2.0 Ga)
Presented by Academician of the NAS of Ukraine O.M. Ponomarenko
The U-Pb age of zircon populations from metadacite of the Huliaipole Suite was determined using the LA-ICP-MS
method as 3085-2850 and 3700-3360 Ma. In addition, two crystals of zircon were discovered with an age of more
than 3800 Ma. According to geological and geochronological data, the Huliaipole Block, 30 × 50 km in size, is com-
posed of rocks and relicts of the Hadean, Archean, and Palaeoproterozoic eons. The oldest nucleus of the Azov Do-
main was probably formed from 3.97 to 3.3 Ga ago. In the Mesoarchean (3.2-3.0 Ga), it became a part of the Middle
Dnieper-Azov-Kursk granite-greenstone terrane. Felsic and intermediate volcanics of the Huliaipole Suite could
have formed due to the melting of the sialic crust, including rocks of the Hadean and Archean age, as a result of the
underplating of basic melts during the formation of the Neoarchean to Paleoproterozoic rift structures..
Keywords: West Azov, Huliaipole block, Hadean, Archean, Paleoproterozoic, Ukrainian Shield, U-Pb age.
49ISSN 1025-6415. Допов. Нац. акад. наук Укр. 2020. № 12
Stages in evolution of Earth’s crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga)
Azov Domain. Some researchers previously suggested that the most ancient granulite-gneissic
complexes of the Azov and Dniester-Bouh domains, as well as the Voronezh Crystalline Massif,
are fragments of one of the most ancient protocratons [2]. Author of work [5] suggested a mo-
del for the autono mous evolution of the “Early Archean cores” of the Azov and Dniester-Bouh
domains, which is confirmed by new geological data.
Geological structure of the study area. The Azov Domain is a part of a larger Mesoarchean
(3.2-3.0 Ga) craton, fragments of which are preserved in the eastern part of the Ukrainian Shield
and as a block of the Kursk Magnetic Anomaly (KMA). In the Neoarchean-Palaeoproterozoic
time, it was fragmented into several tectonic blocks: Vovcha, Remivka, Huliaipole, Bilotserkivka,
and Saltych. The Huliaipole block is 30 × 50 km in size. To the west, north, and east, it is bordered
by the Orekhiv-Pavlohrad structure, the Vovcha and Remivka blocks, respectively (Fig. 1, a).
The Huliaipole and Remivka blocks are separated by the Hauchur fault of northwestern orien-
ta tion, to which the Mesoarchean Kosivtsevo greenstone structure is confined. To the south,
the Huliaipole Block is bordered by the Bilotserkivka Synclinorium and Korsak-Stulneve Anti-
clinorium. Analyzing the geological and structural position of greenstone belts in this area, which
are characterized by a concentric shape and distinct confinement to faults, B.Z. Berzenin was
the first to conclude that they formed on the Paleoarchean granulite-gneissic basement above
the mantle plume [7]. The northern part of the Huliaipole Block is composed of the tonalite-tron d-
hjemite-granodiorite (TTG) rock association, which contains remnants of greenstone structures,
while the central and southern parts are almost completely composed of younger granitoids. In
the central part of the Huliaipole Block, the Huliaipole syncline (3.5 × 9 km) of the NW orien-
tation occurs [8]. Syncline limbs are steeply deeping to the center at an angle of 50-70°. According
to geophysical data, the depth of the fold extent is estimated at 2.1-2.3 km. This structure is com-
posed of volcano-sedimentary rocks of the Huliaipole Suite, about 1700 m thick, unconformably
overlying the Archean TTG. The Huliaipole Suite is subdivided into three subsuites. The lower
one (250 m thick) is composed of two-mica and andalusite-staurolite quartzites and schists;
the middle one (450 m thick) consists of mainly ferruginous quartzites and metavolcanics of
felsic and intermediate composition; the upper one (1000 m thick) is composed of biotite schists,
often graphite-bearing, sometimes high-alumina quartzites and quartzite schists with flysch-like
alternations. To a limited extent, meta-andesites and felsic metavolcanics are also found in the
lower Huliaipole and upper Huliaipole subsuites [6]. The volcanics reach 70 m in thickness.
From the margins to the center of the structure, there is a lateral replacement of ferruginous
quartzites by metavolcanics. In the same direction, in the lower and upper subsuites, clay-rich
facies are replaced by sandy ones. The U-Pb (TIMS) age of the multi-grain detrital zircon frac-
tions from quartzites of the Lower Huliaipole Subsuite is 2.9 ± 0.1 Ga; the time of metamor-
phism of the rocks of the Huliaipole Suite is estimated at 2.14 Ga [9].
The Mesoarchean (3.2-3.0 Ga). The Kosivtseve and Haychur greenstone belts are compo-
sed of metamorphosed rocks of the jaspilite-komatiite-tholeiite association (the Kosivtseve unit),
which is correlated with the Sura Suite of the Konka Series of the Middle Dnieper Do main [10].
Metamorphosed peridotite komatiites of the Kosivtsevo Greenstone Belt belong to the unde-
pleted alumina type: CaO/Al2O3 = 1.23 and Al2O3/TiO2 = 11.61. Ni content in the Kosivtseve
Greenstone Belt peridotite komatiites reaches 841 ppm and Cr content is up to 2540 ppm.
Amphibolites correspond to tholeiitic basalts. The metabasalts are characterized by a flat un-
50 ISSN 1025-6415. Dopov. Nac. akad. nauk Ukr. 2020. № 12
G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker
differentiated pattern of REE (La/Yb)N ~1.0. The REE concentrations in metabasalts of the
Kosivtseve Greenstone Belt is 10 times chondrite content [11].
The TTG intrusions in the northern part of the Huliaipole Block are composed of sodium
diorites and trondhjemites, and quartz diorites and tonalites of the potassium-sodium series.
The U-Pb age of tonalites is 3.0 Ga, and that of trondhjemites is 2.92 Ga. According to Sm-Nd
Fig. 1. a: Schematic geological map of the northern part of the West Azov area.
MD — Middle-Dnieper domain, OPZ - Orekhiv-Pavlohrad zone. 1 — Novo-
pavlivka unit; 2 — Novopavlivka Complex; 3 — West Azov Series; 4 — Auly
Series; 5 — Greenstone belts; 6 — Central-Azov Series; 7 — Huliaipole Suite; 8
— alkaline intrusions; 9 — Paleoproterozoic K-Na granites; 10 — Archean K-Na
gra nites; 11 — plagiomigmatites of the Shevchenko and Dnepropetrovsk com-
plexes; 12 — dating points of tonalites; 13 — dating points of clastogenic
zircons and xenogenic zircons in felsic metavolcanics.
b: Schematic geological map of the Huliaipole brachisyncline [6]. 1 — quar -
t zites, metasandstones; 2 — andalusite-biotite-magnetite shales; 3 — magne-
tite, silicate-magnetite quartzites; 4 — magnetite-silicate quartzites; 5 —
quartz-feldspar-biotite shales; 6 — amphibole-biotite plagiogranites.
c: Schematic column of drill-hole 625-B. 1 — weathering crust of barren
quar tzites; 2 — quartzites with hydromica-limonite-martite (Hyd-Li-Mar,
iron-rich weathering crust); 3 — quartzites with cummingtonite-magnetite
(Cu-Mag); 4 — quartzites with biotite-cummingtonite-magnetite (Bi-Cu-
Mag); 5 — quartzites with biotite-magnetite (Bi-Mag); 6 — metamorphosed
felsic volcanics; 7 — biotite schist
51ISSN 1025-6415. Допов. Нац. акад. наук Укр. 2020. № 12
Stages in evolution of Earth’s crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga)
data, they were derived from a depleted (εNd(T) = 0 to +2.6; TNd(DM) ~3.0 Ga) mantle and do
not have “ancient crustal roots” [11]. Tonalites and trondhjemites are characterized by an ave-
rage and very high degree of REE differentiation - (La/Yb)N = 7.7 and 133, respectively.
The Neoarchean-Palaeoproterozoic (2.8-2.0 Ga). The Neoarchean-Paleoproterozoic for-
mations are represented by volcano-sedimentary rocks of the Huliaipole Suite and granitoids of
the Dobropillya and Anadol complexes.
Granitoids of the Dobropillya Complex are confined to the Haychur and Dobropillya faults
and to the southern margin of the Remivka Block. They are sharply discordant to the structure
of the region and are represented by quartz diorites, plagioclase granites, and granodiorites of
the potassium-sodium series, containing a large amount of pyroxenite, gneiss, and plagioclase
granite xenoliths. According to the geological and geochemical data, the granitoids of the Do-
bropillya Complex were formed due to the melting of the older TTGs with a magma source
characterized by TNd(DM) = 3,0-2,93 Ga [11]. The U-Pb isotope zircon age of granitoids of
the Dobropillya Complex is 2040 Ma [12]. Inherited zircon has an age up to 3400 Ma.
The Anadol Complex. Small intrusions of two-feldspar granites are widespread in the Haychur
area of the Ternuvate structure. In terms of chemical composition, they correspond to the sub-
alkaline chemical group of felsic rocks of the potassium-sodium series. REE are highly differen-
tiated with (La/Yb)N = 16.94, YbN = 8.47, and a prominent negative europium anomaly (Eu/Eu* =
= 0.39). According to geochemical data, two-feldspar granites were derived from a crustal source.
The U-Pb isotope monazite age of two-feldspar granites is 2190 Ma [13].
Felsic metavolcanics of the Huliaipole Suite. In the Huliaipole syncline, intermediate and
felsic metavolcanics are closely associated with the Banded Iron Formation (BIF). Their age has
not yet been studied. Zircon from meta-andesites and felsic metavolcanics of the Huliaipole
Suite is very heterogeneous, which indicates their crustal derivation.
The Hadean-Paleoarchean (4.0-3.4 Ga). The presence of ancient crust in the Huliaipole
Block is indicated by the large number of xenoliths in the granitoids of the Dobropillya Comp-
lex and the ubiquitous presence of xenocrystic zircon [14]. The Paleoarchean age of 3.3 Ga for
xenocrystic zircon (multiple zircon grain method) was determined by [14] and of 3.4 Ga (SHRIMP
U-Pb method) by [12]. A large amount of xenocrystic zircon was also found in me tamorphosed
andesites and dacites of the Huliaipole Suite. This zircon has been dated in this study using the
LA-ICP-MS method. For the most ancient zircons, the age was also confirmed by secondary ion
mass spectrometry (SIMS).
The sampled interval is composed of metadacites (sample 89-388, drill-hole 625-B, int. 424.4-
429.4 meters) (Fig. 1, b, 1, c). The structure of the rock is blastoporphyritic with a lepidograno-
blastic structure of the groundmass (Figs. 2, a, b, c). Phenocrysts are represented by albite. Phe-
nocrysts are often granular and transformed into an aggregate of fine grains. Secondary minerals
in phenocrysts are represented by biotite, sericite, muscovite, chlorite, carbonate, and magnetite.
The bulk is composed (%): quartz + albite 75-77 %, biotite 20-22 %, chlorite — fractions of %,
muscovite — single grains, magnetite — up to 1 %; apatite – 3-5 %, titanomorphite — fractions of
%, zircon — single grains. Quartz and albite form aggregates of isometric grains 0.02 mm in size.
Biotite and chlorite are unevenly distributed, forming clusters of elongated lenticular and irregu-
lar shape. Patchy segregations of magnetite, zircon, and titanomorphite are confined to biotite
accumulations. An interesting feature of the rock is the high content of apatite (up to 5 %).
52 ISSN 1025-6415. Dopov. Nac. akad. nauk Ukr. 2020. № 12
G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker
Fig. 2. Photomicrographs of thin sections of metadacites of the Huliaipole Suite, drill-hole 625-B: a – sample
89-384, depth 424.8 m; b – sample 89-385, depth 427.4 m; c – sample 89-386, depth 428.6 m. Images were taken
using a polarizing microscope ECLIPSE LV100 POL. Crossed analyzers
Fig. 3. Primitive mantle-normalized multi-element diagram for meta-andesites
and metadacites of the Huliaipole Suite — a. Chondrite-normalized REE pat-
tern for meta-andesites and metadacites of the Huliaipole Suite — b
53ISSN 1025-6415. Допов. Нац. акад. наук Укр. 2020. № 12
Stages in evolution of Earth’s crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga)
Geochemistry. In terms of chemical composition, the metavolcanics of the Huliaipole Suite
correspond to low-Mg (0.23-0.35) andesites and dacites of the normal series, potassium-sodium
series (Table 1). On the SiO2-K2O diagram, they fall into the fields of high-K andesites and dac-
ites of the calc-alkaline series. They have high content of Sr (743-816 ppm), Ba (1400-2116 ppm),
and moderate content of Rb (97-103 ppm) (Table 1). The content of transition elements,
Table 1. Chemical composition of metavolcanics of the Huliaipole Suite
% 89-156 89-463 89-381 89-388 ppm 89-156 89-463 89-381 89-388
SiO2 60.70 62.58 63.98 65.70 Ge — — — —
TiO2 0.74 0.46 0.47 0.57 Y 8.19 8.17 7.0 7.5
Al2O3 14.60 13.74 13.36 13.93 Nb 6.49 4.82 5.0 6.7
Fe2O3 0.35 0.72 0.65 1.41 Zr 160 116.4 162.6 190
FeO 4.70 3.60 3.38 3.38 Hf — 3.48 3.3 4.9
MnO 0.08 0.06 0.05 Сл U 1.41 1.83 1.4 1.4
MgO 1.90 2.26 1.24 1.79 Th 6.71 7.25 5.6 6.5
CaO 5.10 3.96 3.50 3.62 Sn — 0.70 — 1.1
Na2O 4.30 5.34 3.78 3.78 Sb — 0.12 — 0.25--
K2O 3.52 3.60 6.00 3.18 La 32.50 29.05 35.9 38.3
Sобщ 0.30 0.23 0.24 0.13 Ce 62 57.07 68.1 76.0
P2O5 0.36 0.24 0.10 0.24 Pr 7.07 6.36 7.60 7.9
CO2 2.69 2.24 0.07 1.30 Nd 26.60 24.87 26.7 29
H2O- Сл. 0.08 0.12 Сл. Sm 4.75 4.15 4.52 4.5
LOI 0.34 0.56 2.64 0.59 Eu 1.70 1.26 1.23 1.1
Sum 99.68 99.67 99.58 99.62 Gd 3.61 3.81 3.14 3.4
#mg 0.27 0.35 0.23 0.28 Tb 0.49 0.39 0.36 0.41
Ppm Dy 1.98 2.11 1.45 1.6
Cs — 18.53 — 4.8 Ho 0.30 0.38 0.23 0.26
Li — 14.88 — 23 Er 0.73 1.09 0.60 0.66
Be — 1.94 — 1.4 Tm 0.092 0.14 0.08 0.088
Rb 97.10 96.90 102.6 174 Yb 0.51 0.95 0.53 0.54
Sr 816 742.9 812.1 647 Lu 0.072 0.14 0.06 0.08
Ba 1400 1953 2116 2327 Mo — 0.83 0.2 0.49
V 64.50 64.78 67 42.5 Ag — 70.43 <0.1 —
Cr 21.30 70.42 — 41.7 Ta 0.37 — 0.3 0.42
Co 7.29 12.55 9.6 7.5 Pb — 17.70 9.5 19.2
Ni 15 33.61 27.2 19.3 W — 0.44 — 7.5
Cu — 26.93 17.4 30.2 (La/Yb)N
45.7 21.9 48.6 50.9
Zn — 70.31 60 58.2 Eu/Eu* 1.26 0.97 1.0 0.97
Ga — 47.55 — 16.6 Nb/La 0.20 0.17 0.14 0.17
As — 2.13 — 0.48 Nb/Ce 0.11 0.08 0.07 0.09
Sc — 18.53 — 4.1 Th/Yb 13.2 7.4 10.6 12
N o t e: 1 — meta-andesite, drill-hole 636-B, depth 384.5-384.7 m (sample 89-156); 2 — meta-andesite, drill-hole
795-B, depth 392-395.7 m (sample 89-463); 3 — meta-andesite, drill-hole 625-B, depth 424.4-429.4 m (sample
89-388); 4 — metadacite, drill-hole 625-B (sample 89-381). Silicate rock analyses were carried out at IGMOF of
the NAS of Ukraine, Kyiv. Contents of rare and trace elements were determined using the ICP-MS method at
IMTM RAS, Chernoholovka, Russia. #mg = MgO/(MgO + FeO*).
54 ISSN 1025-6415. Dopov. Nac. akad. nauk Ukr. 2020. № 12
G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker
Fig. 4. a: Cathodoluminescence images of the studied zircon crystals from metadacites of the Huliaipole Suite.
Shown are numbers for analyzes and ages based on isotopic ratio 207Pb/206Pb (Drill-hole 625-B, depth 424,4 -
429,4 meteоrs, sample 89-388).
b: U-Pb diagram with concordia for zircons from metadacites of the Huliaipole Suite (Drill-hole 625-B, depth
424,4 - 429,4 meters, sample 89-388).
c: Hf isotope systematics of zircons from metadacites of the Huliaipole Syncline. Zircons from other rock com-
plexes of the Ukrainian Shield are shown for comparison. 1 — Eoarchaean enderbite of the Dniester-Bouh Series
[2]; 2 — mafic granulite of the Dniester-Bouh Series [15]; 3 — Archaean metasediments of the Azov Domain [16];
4 — Bouh Series quartzite [9]; 5 — Metavolcanics of the Huliaypole Suite
55ISSN 1025-6415. Допов. Нац. акад. наук Укр. 2020. № 12
Stages in evolution of Earth’s crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga)
Ni (15-33.6 ppm) and Cr (21.3-70.42 ppm), are close to their content in TTGs. Negative ano-
malies of Nb and Ti are highlighted on the multi-element diagram (Fig. 3, a). Rare earth elements
in meta-andesites and metadacites are highly differentiated — (La/Yb)N = 21.9–50.9 (Fig. 3, b).
The sample 89-156 shows a prominent positive europium anomaly, Eu/Eu* = 1.26; the rest of
sample lack positive europium anomaly. The high Th/Yb ratio (7.4-13.2) and low Nb/La
(0.14-0.20) indicate contamination with crustal material (Table 1). Geochemical data indicate
derivation of metavolcanics of the Huliaipole Suite from the crustal magma source bearing
ancient TTGs.
Geochronology. The LA–ICP–MS method was used to determine the U–Pb age and Hf iso-
topic composition in zircons from metadacites of the Huliaipole Suite (sample 89-388) (Fig. 4, a).
A total of 36 zircon crystals was analyzed (Table 2). The age of the most ancient zircons was also
confirmed by dating with the secondary ion mass spectrometry (SIMS) method.
According to the data obtained, two main populations of zircon can be distinguished (Fig. 4, b).
The first population includes a group of zircons with an age in the range of 3085-2850 Ma. The Hf
isotopic composition varies within wide limits: 5 crystals have εHf values from 6.2 to –0.5;
other 6 have values from –7.5 to –21 (Fig. 4, c). Thus, zircons of this group come from rocks of
different genesis: some of them were of juvenile origin, while others were formed as a result of
the processing of the ancient crust. The second population includes zircons with an age of
3700-3360 Ma, which also have variable Hf isotope characteristics: from juvenile (εHf up to 1.6)
and negative εHf values (down to –7.7 at an age of 3705 Ma).
In addition, two zircon crystals with the age of more than 3800 Ma were found (3805 Ma
with εHf = –3.3, and 3971 Ma with εHf = –1.3). These zircons are the most ancient found in
the Ukrainian Shield. Their isotopic characteristics indicate the presence of Hadean material
within the Azov Domain of the Ukrainian Shield. The minimum model age for the crystalliza-
tion of this material, calculated at Lu/Hf = 0 for zircons with the lowest εHf values in each age
population, is about 4.1 Ga (Fig. 4, c).
Discussion of the results. The two main zircon populations found in metavolcanics of the
Huliaipole Suite are similar in their U-Pb and Hf isotopic characteristics to zircons from the
Archean metasedimentary rocks of the Soroki Greenstone Belt of the Azov Domain [2] as well as
zircons from quartzites of the Bouh Group of the Dniester-Bouh Domain of the Ukrainian Shield
[17]. At the same time, the older (3700-3360 Ma) zircon population corresponds in age and iso-
topic composition to zircons from the Eoarchean enderbites of the Dniester-Bouh Domain [2, 17].
Another intriguing observation: similarly to the iron-bearing metasedimentary successions
of the Middle Dnieper Domain, no zircons younger than ca. 2800 Ma were found in the green-
stone belts of the Azov Domain, and in the metavolcanics of the Huliaipole Suite (e.g., [4, 18],
which supports common geological history of these two domains in the Neoarchean and Paleo-
proterozoic.
Finally, among the detrital zircons from the metasedimentary rocks of the Soroki Greenstone
Belt of the Azov Domain [2], one zircon crystal corresponds to the most ancient zircon crystals
from the metavolcanic rocks of the Huliaipole Suite in terms of isotopic and geochemical charac-
teristics, and has a minimum hafnium model age of about 4.1 Ga. Thus, the Azov Domain of the
Ukrainian Shield holds high promise for the search for Hadean zircons and the study of the early
evolution of Earth.
56 ISSN 1025-6415. Dopov. Nac. akad. nauk Ukr. 2020. № 12
G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker
Table 2. Results of U-Pb isotope dating of zircons from metadacites of the Huliaipole Suite arranged
in descending order of 207Pb/206Pb ages (Drill-hole 625-B, depth 424.4-429.4 meters, sample 89-388)
# analysis
Concentration,
ppm
Isotope ratio
U Th Th/U 207Pb/235U 2σ 206Pb/238U 2σ Rho 207Pb/206Pb 2σ
89-388-18 176 109 0.62 49.900 2.507 0.84 0.03 0.98 0.424 0.011
89-388-29 61 38 0.62 42.280 1.157 0.79 0.02 0.98 0.389 0.008
89-388-17 165 96 0.58 44.000 1.409 0.81 0.02 0.97 0.388 0.008
89-388-14 148 76 0.51 37.430 1.096 0.77 0.02 0.99 0.356 0.007
89-388-16 188 73 0.39 37.060 0.923 0.76 0.02 0.99 0.356 0.007
89-388-22 295 74 0.25 37.080 0.980 0.75 0.02 0.98 0.354 0.007
89-388-20 171 136 0.79 38.590 1.232 0.79 0.02 0.98 0.354 0.007
89-388-9 276 85 0.31 36.400 2.412 0.76 0.05 0.99 0.350 0.007
89-388-25 245 15 0.06 36.250 0.910 0.74 0.02 0.96 0.349 0.007
89-388-34 490 7 0.01 33.720 1.009 0.71 0.02 0.99 0.339 0.007
89-388-10 357 122 0.34 31.390 0.822 0.70 0.02 0.79 0.329 0.007
89-388-6 48 16 0.33 34.070 0.984 0.79 0.02 0.99 0.314 0.006
89-388-1 70 28 0.4 31.250 0.938 0.72 0.02 0.98 0.313 0.006
89-388-5 117 83 0.71 31.060 0.843 0.72 0.02 0.98 0.313 0.006
89-388-23 60 23 0.38 32.040 1.009 0.74 0.02 0.99 0.313 0.006
89-388-30 234 170 0.73 30.330 0.957 0.70 0.02 0.94 0.310 0.006
89-388-27 209 153 0.73 30.350 0.686 0.71 0.02 0.99 0.305 0.006
89-388-7 167 39 0.23 30.480 1.120 0.73 0.03 0.97 0.303 0.006
89-388-13 624 24 0.04 25.900 0.748 0.63 0.02 0.96 0.300 0.006
89-388-31 163 76 0.47 28.060 0.752 0.69 0.02 0.98 0.291 0.006
89-388-21 201 79 0.39 26.330 0.876 0.68 0.02 0.96 0.282 0.006
89-388-35 68 52 0.76 25.920 1.030 0.67 0.03 0.99 0.280 0.006
89-388-33 193 77 0.40 20.120 0.706 0.59 0.02 0.97 0.245 0.005
89-388-26 230 244 1.07 18.620 0.820 0.56 0.03 1.00 0.235 0.005
89-388-15 187 63 0.34 19.300 0.471 0.60 0.01 0.93 0.234 0.005
89-388-12 426 38 0.09 16.020 0.825 0.52 0.02 0.95 0.227 0.006
89-388-3 97 38 0.39 16.850 0.451 0.55 0.01 0.52 0.222 0.006
89-388-28 139 32 0.23 17.100 1.832 0.56 0.06 1.00 0.218 0.005
89-388-4 129 57 0.44 16.500 0.542 0.56 0.02 0.82 0.216 0.006
89-388-2 258 119 0.46 15.500 1.336 0.53 0.05 1.00 0.214 0.004
89-388-32 512 441 0.86 16.590 0.520 0.56 0.02 1.00 0.212 0.004
89-388-11 105 5 0.05 13.470 0.450 0.47 0.02 0.97 0.208 0.004
89-388-8 63 81 1.28 15.610 0.615 0.56 0.02 0.99 0.203 0.004
89-388-19 46 71 1.54 15.680 0.485 0.55 0.02 0.98 0.203 0.004
89-388-24 39 41 1.05 15.720 0.414 0.56 0.01 0.94 0.202 0.004
57ISSN 1025-6415. Допов. Нац. акад. наук Укр. 2020. № 12
Stages in evolution of Earth’s crust recorded by the Huliaipole block of the West Azov area (4.0-2.0 Ga)
Isotopic age, Ma
208Pb/232Th 2σ 207Pb/235U 2σ 206Pb/238U 2σ 208Pb/232Th 2σ 207Pb/206Pb 2σ
0.213 0.006 3986 49 3940 100 3897 78 3997 25
0.198 0.006 3831 20 3739 59 3644 84 3865 4
0.211 0.006 3863 25 3832 66 3866 81 3862 7
0.212 0.007 3704 21 3662 56 3888 92 3734 5
0.215 0.005 3695 15 3637 36 3940 50 3733 4
0.192 0.006 3695 17 3609 47 3551 72 3726 4
0.209 0.006 3740 22 3748 58 3831 79 3722 5
0.217 0.019 3667 62 3620 170 4050 340 3705 9
0.229 0.011 3677 17 3575 43 4160 170 3704 6
0.169 0.014 3601 22 3464 66 3150 240 3656 7
0.209 0.010 3531 17 3411 50 3830 150 3611 15
0.218 0.008 3611 21 3749 59 3980 120 3539 8
0.197 0.008 3526 22 3510 62 3630 110 3538 6
0.201 0.006 3520 18 3501 48 3707 65 3537 3
0.188 0.008 3551 24 3551 66 3490 130 3534 7
0.187 0.005 3496 24 3432 62 3471 65 3520 10
0.185 0.004 3498 10 3462 33 3436 33 3498 3
0.198 0.006 3500 30 3513 88 3654 71 3486 11
0.197 0.007 3342 20 3141 53 3635 89 3471 5
0.183 0.005 3421 18 3394 51 3395 59 3423 5
0.177 0.005 3358 27 3323 57 3298 67 3375 8
0.182 0.009 3341 34 3310 100 3370 150 3363 7
0.159 0.004 3096 29 2999 77 2976 50 3152 15
0.119 0.023 3019 39 2902 95 2250 420 3086 4
0.182 0.005 3056 14 3031 35 3371 64 3078 7
0.153 0.006 2885 43 2712 64 2884 99 3029 26
0.206 0.010 2926 17 2837 33 3790 150 2993 27
0.166 0.013 2920 110 2860 240 3100 220 2962 12
0.121 0.005 2905 25 2864 60 2308 78 2953 28
0.060 0.009 2838 72 2720 180 1170 170 2936 6
0.153 0.005 2910 24 2875 58 2879 75 2920 3
0.067 0.013 2712 26 2511 41 1320 250 2892 11
0.163 0.006 2851 33 2860 76 3058 79 2848 7
0.150 0.004 2856 23 2839 52 2826 58 2852 9
0.152 0.004 2860 16 2878 38 2864 44 2840 13
58 ISSN 1025-6415. Dopov. Nac. akad. nauk Ukr. 2020. № 12
G.V. Artemenko, L.V. Shumlyanskyy, S.A. Wilde, M.J. Whitehouse, A.Yu. Bekker
Conclusions. The Huliaipole Block of the Azov Domain of the Ukrainian Shield carries evi-
dence for a protracted geological evolution from the Hadean to the Palaeoproterozoic. The Azov
Domain indicates existence of the cratonic nucleus formed from 3.97 to 3.3 Ga ago. In the Meso-
archean (3.2-3.0 Ga), the Huliaipole Block was a part of the Middle-Dnieper-Azov-Kursk gran-
ite-greenstone terrane. Felsic and intermediate volcanic rocks of the Huliaipole Suite could have
formed due to the melting of the sialic continental crust, including components of the Hadean and
Archean age, as a result of the underplating by mafic magmas during the formation of Neoarchean-
Paleoproterozoic extension-related rift structures.
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Received 16.11.2020
Г.В. Артеменко 1, Л.В. Шумлянський 1, 2,
С.А. Вайде 2, М.Дж. Вайтхаус 3, А.Ю. Беккер 4
1 Інститут геохімії, мінералогії та рудоутворення ім. М.П. Семененка НАН України, Київ
2 Картинський університет, Факультет наук про Землю та планети, Перт, Австралія
3 Шведський музей природи, Стокгольм, Швеція
4 Факультет наук про Землю та планети, Каліфорнійський університет, Ріверсайд, США
E-mail: regulgeo@gmail.com, leonid.shumlyanskyy@curtin.edu.au,
S.Wilde@curtin.edu.au, martin.whitehouse@nrm.se, andreyb@ucr.edu
ЕТАПИ ФОРМУВАННЯ ЗЕМНОЇ КОРИ
НА ПРИКЛАДІ ГУЛЯЙПІЛЬСЬКОГО БЛОКА
ЗАХІДНОГО ПРИАЗОВ’Я (4,0—2,0 млрд років)
Методом LА-ICP-MS визначено U-Pb вік популяцій циркону з метадацитів гуляйпільської світи — 3085—
2850 і 3700—3360 млн років. Крім того, виявлено два кристали циркону віком понад 3800 млн років. Згідно
з геологічними і геохронологічними даними, Гуляйпільський блок, який має розміри 30 × 50 км, складений
породами і їх реліктами гадейського, архейського і палеопротерозойського еонів. Найдавнішим фунда-
ментом Приазовського мегаблока є, ймовірно, породи нуклеарної структури, яка формувалася від 3,97
до 3,3 млрд років. У мезоархеї (3,2—3,0 млрд років) вона стала частиною Середньопридніпровсько-При-
азовсько-Курського граніт-зеленокам’яного терейну. Вулканіти кислого і середнього складу гуляйпіль-
ської світи могли утворитися внаслідок плавлення порід сіалічної кори, що включала породи гадейського
і архейського віку, в результаті андерплейтингу базитових розплавів під час формування неоархей-палео-
протерозойських рифтогенних структур.
Ключові слова: Західне Приазов’я, Гуляйпільський блок, гадей, архей, палеопротерозой, Український щит,
U-Pb вік.
|