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GEODYNAMICS & TECTONOPHYSICS
PUBLISHED BY THE INSTITUTE OF THE EARTH'S CRUST SIBERIAN BRANCH OF RUSSIAN ACADEMY OF SCIENCES
ISSN 2078-502X
2019 VOLUME 10 ISSUE 1 PAGES 79-99
https://doi.org/10.5800/GT-2019-10-1-0405
A review of Early Permian (300-270 Ma) magmatism in Eastern Kazakhstan and implications for plate tectonics
and plume interplay
S. V. Khromykh1, 2, P. D. Kotler1, 2, A. E. Izokh1, 2, N. N. Kruk1
1 V.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of RAS, Novosibirsk, Russia
2 Novosibirsk State University, Novosibirsk, Russia
Abstract: The history of the Central Asian Orogenic Belt (CAOB) was marked by several major events of magmatism which produced large volumes of volcanic and intrusive (mafic-ultramafic and granitic) rocks within a relatively short time span (30-40 Ma) over a vast area. The magmatic activity postdated the orogenic stages of accretionary-collisional belts in Central Asia and likely resulted from the impact of mantle plumes that formed Large Igneous Provinces (LIPs). The formation of the Tarim-South Mongolia LIP at 300-270 Ma is the best known among the major Permian events of basaltic and granitic magmatism. Early Permian igneous rocks (volcanic, subvolcanic and intrusive suites that vary from ultramafic to felsic compositions) of the same age range (300 to 270 Ma) have been recently found also in Eastern Kazakhstan, within the late Paleozoic Altai collisional system. The compositions and ages of the rocks suggest that the Eastern Kazakhstan magmatism was the northward expansion of the Tarim LIP. The spread of the Tarim LIP was apparently facilitated by lithospheric extension after the Siberia-Kazakhstan collision. The extension led to rheological weakening of the lithosphere whereby deep mantle melts could penetrate to shallower depths. The early Permian history of Eastern Kazakhstan was controlled by the interplay of plate tectonic and plume processes: plate-tectonic accretion and collision formed the structural framework, and the Tarim mantle plume was a heat source maintaining voluminous magma generation.
Key words: Central Asian Orogenic Belt; post-orogenic magmatism; Tarim mantle plume; mantle-crust interaction
RESEARCH ARTICLE Received: September 12, 2018
Revised: December 14, 2018 Accepted: January 12, 2019
For citation: Khromykh S.V., Kotler P.D., Izokh A.E., Kruk N.N., 2019. A review of Early Permian (300-270 Ma) magmatism in Eastern Kazakhstan and implications for plate tectonics and plume interplay. Geodynamics & Tectonophysics 10 (1), 79-99. doi:10.5800/GT-2019-10-1-0405.
Раннепермский (300-270 млн лет) магматизм Восточного Казахстана как результат сочетания плейт- и плюм-тектонических факторов
С. В. Хромых1- 2, П. Д. Котлер1- 2, А. Э. Изох1- 2, Н. Н. Крук1
1 Институт геологии и минералогии им. В.С. Соболева СО РАН, Новосибирск, Россия
2 Новосибирский национальный исследовательский государственный университет, Новосибирск, Россия
Аннотация: В истории развития крупнейшего Центрально-Азиатского складчатого пояса (ЦАСП) выявлены несколько периодов крупномасштабной эндогенной активности, характеризующихся проявлениями значительных объемов вулканических и интрузивных (как базитовых, так и гранитоидных) пород на обширных территориях в сравнительно короткие временные интервалы (30-40 млн лет). Эти вспышки магматической активности обычно происходят после завершения аккреционно-коллизионных процессов в складчатых системах и рассматриваются как результат воздействия мантийных плюмов на литосферу - крупные изверженные провинции. Одним из ярких примеров является Тарим-Южномонгольская крупная изверженная провинция (300-270 млн лет назад), характеризующаяся широким развитием базитового и гранитоидного магматизма в западной части ЦАСП. Исследования последних лет показали, что в Восточном Казахстане, в пределах Алтайской коллизионной системы герцинид, широко распространены как базитовые, так и гранитоид-ные комплексы раннепермского возраста (300-270 млн лет). В приведенном кратком обзоре показано, что особенности состава и условия формирования этих магматических ассоциаций позволяют рассматривать их как результат северо-западного распространения влияния Таримской крупной изверженной провинции. Распространение этого термического возмущения в литосфере, по-видимому, стало возможным благодаря пост-орогеническому растяжению после коллизии Сибирского и Казахстанского континентов. Реологическое ослабление литосферы позволило глубинным расплавам проникать в литосферную мантию, образовав крупные очаги базитовых магм. Таким образом, современный геологический облик и металлогеническая специфика территории Восточного Казахстана является результатом плейт-тектонических процессов постороге-нического растяжения на фоне повышенного термического градиента в мантии, вызванного активностью Таримского мантийного плюма.
Ключевые слова: Центрально-Азиатский складчатый пояс; посторогенный магматизм; Таримский плюм; мантийно-коровое взаимодействие
1. Introduction
The Central Asian Orogenic Belt (CAOB) is the largest accretionary structure in the Earth's history, also known as Altaids [$engor et al., 1993], formed by closure of the Paleoasian Ocean. The Altaid tectonic collage includes numerous terranes of different origin amalgamated by multiple accretionary and collisional events in tectonic settings changing from compression to extension and shear [$engor et al., 1993; Dobretsov, 2003; Windley et al., 2007; Levashova et al., 2009; Xiao et al., 2010; Xiao, Santosh, 2014]. Its history included several major events of magmatism which produced significant volumes of volcanic and intrusive (mafic-ultramafic and granitic) rocks in a relatively short time span (30-40 Ma) over a large area. The magmatic activity postdated the orogenic stages in the evolution of accretionary-collision systems. From the viewpoints of plate tectonics, the post-orogenic magmatism is caused by post-orogenic lithospheric extension as a result of
its delamination [Xiao et al., 2008; Xiao, Santosh, 2014; Konopelko et al., 2018] or results from active transten-sional strike-slip tectonics accompanied by upwelling of the asthenosphere [Seltmann et al., 2011; Wang et al., 2014] or breaking of subducted oceanic plate (slab break-off) [Konopelko et al., 2017]. The alternative viewpoint for large-scale magmatism in accretionary-collision systems is the impact of mantle plumes. The plume activity leading to the formation of Large Igneous Provinces (LIPs) [Ernst et al., 2005; Bryan, Ernst, 2008; Ernst, 2014] can account for a number of Paleozoic magmatic events in CAOB: (1) early Paleozoic, with a late Cambrian - early Ordovician LIP in the Altai, Sayan and Western Mongolia regions [Izokh et al., 2010; Dobretsov, 2011; Vladimirov et al., 2013]; (2) middle Paleozoic, with a Devonian LIP in the Minusa basin and the Vilyui rift in East Siberia [Vorontsov et al., 2013; Kiselev et al., 2014]; and (3) late Paleozoic, with Permian LIPs in Central Asia. Large-scale mafic and granitoid magmatism in Permian time produced the
Tarim-South Mongolia LIP at 300-270 Ma [Zhang et al., 2010; Wei et al., 2014; Xu et al., 2014; Yu et al., 2017]; the Barguzin LIP at 330-280 Ma [Kuzmin, Yarmolyuk, 2014; Yarmolyuk et al., 2014]; and the Khangai LIP at 270-245 Ma [Yarmolyuk et al., 2014] (Fig. 1).
The Tarim - South Mongolia Province is the largest area of diverse late Paleozoic magmatism in Central Asia, with voluminous continental flood basalts and other volcanic rocks found within the Tarim continental block [Yu et al., 2011; Li et al., 2014, 2017]. As confirmed by recent studies, the Tarim LIP spreads over the regions of South Mongolia [Kozlovsky et al., 2015], Chinese Altai [Zhang et al., 2014], North-Western Xinjiang [Pirajno et al., 2011; Gao et al., 2014], and Tien Shan [Seltmann et al., 2011], as well as into Eastern Kazakhstan.
2. Late Paleozoic Altai accretionary-collisional system
Eastern Kazakhstan is part of the Altai collisional system in the western Central Asian Orogenic Belt. The system formed in late Paleozoic as a result of an oblique collision of Siberia with the Kazakhstan composite terrane [Vladimirov et al., 2003, 2008; Xiao et al., 2010]. In Devonian through early Carboniferous time, the paleocontinents of Siberia and Kazakhstan were separated by the Ob'-Zaisan oceanic basin (a fragment of the western Paleoasian Ocean) with subduction involving continental blocks (Rudny-Altai and Zharma-Saur terranes) on its margins. Remnant oceanic crust and subduction-related sedimentary and volcanic rocks can be found as numerous fault blocks within the Central part of Altai collisional system [Safonova et al., 2012, 2018]. Collisional crust thickening and orogeny show up in the presence of late Carboniferous continental molasse with basal conglomerates in several intermontane basins (Fig. 2). The post-orogenic (latest Carboniferous - earliest Permian) tectonic activity occurred mainly as strike-slip motions [Buslov, 2011].
The igneous rocks of Eastern Kazakhstan, including various ultramafic to felsic volcanic, subvolcanic and intrusive suites, were studied in detail in the 1970s [Shcherba et al., 1976, 1998; Ermolov et al., 1977, 1983; Lopatnikov et al., 1982]. Variations in their forms and compositions allow suggesting their origin at different evolution stages, from the early Carboniferous to the Triassic. The studies of magmatism in Eastern Kazakhstan remained suspended in the 1990s - 2000s, until we resumed the work in 2005 at a more advanced level. Since then, a wealth of data has been obtained on the compositions and ages of igneous rocks in the region, which bracket the magmatic activity between 300 and 270 Ma, or within the early Permian (Fig. 2). The results from some units have been reported in recent
publications [Khromykh et al., 2011, 2013, 2014, 2016, 2017a, 2017b, 2018]. In this paper, we present a brief overview of the obtained data with implications for post-collisional processes in the region.
3. Volcanic basins and structures (297-290 Ma)
There are several volcanic basins filled with subal-kaline basalts, basaltic andesites and andesites in the central part of the studied region (Fig. 2) and some basins filled with dacites and rhyolites in the southeastern areas. Some basins contain also small subvolcanic bodies of andesite and dacite porphyries.
Mafic volcanic rocks contain relatively high alkalis (Na2O+K2O from 3.2 to 9.2 wt %), potassium (K2O up to 4.9 wt %), alumina (A^Os from 14 to 23 wt. %), phosphorus (P2O5 up to 1 wt. %) and titanium (TiO2 up to 1.5 wt. %), as well as Ba, Zr and LREE (Fig. 3, a-d). Trachydacites from the Daubai and Tyureshoke basins have LA-ICP-MS U-Pb zircon ages of 297±1 Ma and 290±4 Ma, respectively (Fig 3, e-f). Felsic volcanics in some basins coexist with subvolcanic garnet dacites and clinopyroxene andesites derived from magmas that were generated in the lower crust at ~10 kbar and 1000 to 1200 °C by partial melting of the crustal substrate under the effect of hot mantle melts [Khromykh et al., 2011].
4. SUBALKALINE GABBRO AND PICRITES (293-280 MA)
There are about fifty small intrusions that consist of gabbro, or gabbro and picrites (Fig. 4) and belong to the (1) Argimbai plagiosyenite-gabbro (older) and (2) Maksut gabbro-picrite (younger) complexes. The Argimbai gabbro was dated at 293±2 Ma by the SHRIMP-II U-Pb method on zircons. The Maksut gabbro and picrites have an Ar-Ar age of 280±3 Ma on biotite (3 samples from 3 different intrusions) and amphibole (1 sample from the Maksut intrusion) [Khromykh et al., 2013].
Both the Argimbai gabbroic rocks and the Maksut picrites have high contents of alkalis (5.2 to 7.8 wt. % and 2 to 5 wt % Na2O+K2O in the two complexes, respectively), relatively high potassium (up to 2.8 wt. % and 1.3 wt. % K2O, respectively) and phosphorus (to 0.8 wt. % and 0.3 wt. % P2O5, respectively). The Argimbai gabbro typically contain up to 1000 ppm LREE and Ba, 980 ppm Sr, 350 ppm Zr, and 25 ppm Rb. The concentrations of trace and rare-earth elements in the Maksut picrodolerite and picrite are lower than in the Argimbai gabbro but higher than in ultramafic rocks (up to 280 ppm Ba, 830 ppm Sr, 110 ppm Zr, and 8 ppm Rb) (Fig. 5). Mineralization in the two complexes [Mekhonoshin et al., 2017] consists of Ti (Argimbai
Fig. 1. Simplified tectonics of the Central Asian Orogenic Belt (after [Wind ley etal., 2007; Levashova etal, 2009; Xiao etal., 2010]) and location of Permian Large Igneous Provinces (after [Yarmolyuk et al., 2014]).
Рис. 1. Упрощенная тектоническая схема Центрально-Азиатского складчатого пояса (по [Windley et al, 2007; Levashova et al., 2009; Xiao et al, 2010]) и пермских крупных изверженных провинций (по [Yarmolyuk et al., 2014]).
Platforms
Novosibirsk
Caledonian
subduction-accretion Hercynian - comp|ex
Mesozoic
Quaternary sediments Faults
Irkutsk
■Kamei
Tuva - Mongolia massif
Khangai
T.À?ëa~~
Ulaanbaat
Junggar basin
iJrútriqi
i an/Orogemc
~ Vji--
/»Aksu
FORM
Mongol
¡¡shan Orpgenic
Ust'-Kamenogorsk (Oskemen)
Г27Б+Т
I 267±1
284±4|
29Ш
297+T
279±ЗЩ. I2Ô3±zH
ЧШМ
290+11 ' o^l 292±1
subduction and \
_ accretionary complexes:
island arcs, ophiolites, etc. (O-S-D)
shallow-water clastic sediments (C,)
О
CD О
Q.
<
S
Ш
3
subduction gabbro and diorites, Saur complex (C,)
subduction granodiorites and granités, Bugaz complex (C,)
basins filled by molasse with basal conglomerates (C2)
andesite and basalt (green) or dacite and rhyolite (orange) lavas in basins (P,)
gabbro and picrite intrusions (P,)
gabbro-granite intrusions of complex structure (P,)
+ + + + + + + + + + ■
granodiorites and granites of Suite 1 (P,)
granites and leucogranites of Suite 2 (P,)
post-batholith dike belts (P,_2)
faults
Cenozoic sediments
Fig 2. Sketch map of the central part of Altai collisional system (Eastern Kazakhstan], after [Khromykh et al., 2017b], Subduction-accretion-collision complexes are in gray shades; post-orogenic magmatic complexes are coloured.
Рис. 2. Расположение посторогенных магматических комплексов (выделены цветом] на схеме геологического строения центральной части Алтайской коллизионной системы (Восточный Казахстан), по [Khromykh et al., 2017Ь]. Предшествующие геологические комплексы аккреционно-коллизионной стадии показаны серым фоном.
о ■а
<
о с
3
ф
"О
ш
ю ф
(Л
Na20+KA wt %
Foidite
20
10-
5-
2-
Zr/Y (Ь)
Zr- Zr/Y [Pearce and Norry, 1979\
□ □
•* •
□
/ • • /
P 0 thin-Plate
• * / / Basalts
Island Arc / / / /' Mid-Ocean
Basalts /' / --------_/-------'' ' Ridge Basalts
'----------- Zr, ppm
rock/chondrite
90 10 1000
100-
10-
Daubai basin Tyureshoke basin
La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
100-
10-
CsRbBaTh U K TaNbLacgSr^Hf^Sm^Gd-rbDy-n Y ErYbLu
^gj data^oint error ellipses are 2o
•Q
a.
ш
0.049 -
0.048 -
0.047 -
0.046 -
0.045 -0.30
Daubai basin
""РЬГи
Concordia Age = 296.9±0.9 Ma (2s, decay-const, errs included) MSWD (of concordance) = 6.4
0.32
0.34
0.36
0.38
0.050
0.048
0.046
0.044
0.042
^ data-point error ellipses are 2a
Tyureshoke basin
0.30
™РЬГи
0.Ï32
Concordia Age = 290.4±4.1 Ma
(2s, decay-const, errs included) MSWD (of concordance) = 0.44
0.34
0.36
0.38
I Fig. 3. Basalts and andesites from volcanic basins in the TAS (a) and Zr-Zr/Y (b) diagrams; REE (c) and trace-element (d) compositions of volcanic rocks; U-Pb ages of andesite from the Daubai basin (e) and dacite from the Tyureshoke basin f).
Рис. 3. Составы базальтов и андезитов из вулканических прогибов на классификационных диаграммах TAS (a) и Zr-Zr/Y (b); спектры распределения РЗЭ (c) и мультиэлементные спектры (d) для вулканических пород; U-Pb диаграммы с конкордией для цирконов из андезитов Даубайского прогиба (e) и из дацитов Тюрешокинского прогиба f).
U-Pb age of Argimbai complex
Gabbro, Kokpekty massif Concordia Аде = 293.2±2.0 Ma (2s, decay-const, errs Included) MSWD (of concordance) = 2.6 J
л а. " i
310 aÓQ ~ 29С^Я/ 280
И8и/2МРЬ
Cenozoic sediments
350т
300
250
ra
í> 200
а: ? 150
100
50
n
0
350т
300
250
ra
200
o> 1h()
<
100
50
Ar-Ar ages of Maksut complex
Plateau age = 280.5±2.9 Ma
Integrated age = 278.3±2.9 Ma
Sp. CC-17-3, biotite, picrite, Kokpekty massif
10 20 30 40 50 60 70 80 90 100
Integrate Plateau age = 280.7±3 Ma
d age = 278.8±3 Ma Sp. X-914, biotite, picrite, Tastau massif
350
300
250
ra ?nn
Ь
а> 150
< 100
50
а
0
500т
450
400
350
ra 5 300
0) 250
200
150
100
50
oi
Plateau age = 280.1±3.1 Ma
Integrated age = 278.8±2.9 Ma
Sp. 1217-5, biotite, picrite, Maksut massif
10 20 30 40 50 60 70 80 90 100
Sp. 1217-5, hormblende, picrite, Maksut massif
Plateau age = 278.6±3.3 Ma
Integrated age = 279.1±3.9 Ma
0 10 20 30 40 50 60 70 80 90 100 MAr released, %
Ш
| Fig. 4. Simplified geology of the Argimbai intrusive area [Khromykh et al, 2013], and ages of gabbro and picrites of the Argimbai and Maksut complexes.
Рис. 4. Схема геологического строения Аргимбайского интрузивного пояса [Khromykh et al, 2013] и результаты определения возраста для габбро и пикритов аргимбайского и максутского комплексов.
о
(Б О а
с □
ш 3
о
3
■и
<
О с 3
(О
VI VI
с
(В
-о
ш со
(Б (Л
CaO
■V V
L
И ~ E* ♦
♦
#
Si02
50
60
gabbro
' of Argimbai complex
picrites and gabbro ' of Maksut complex
CsRbBaThU К TaNbLaCeSrNdHfZrSmEuGdTbDy-n Y Er Yb Lu
La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Fig. 5. Compositions of the Argimbai gabbro and the Maksut picrites and gabbro. Рис. 5. Составы габбро аргимбайского комплекса, габбро и пикритов максутского комплекса.
gabbro) and Cu-Ni sulfides and precious metals (Maksut picrites). The intrusions similar in composition, age and mineralization are manifested in the south-eastern extension of these complexes, in Chinese Altai (Kalatongke) and East Tianshan (Huangshan-Jing and others) [Polyakov et al., 2008; Pirajno et al., 2011].
5. Complex gabbro-granite intrusions (290-280 Ma)
Some gabbro-granite intrusions (Preobrazhenka, Tastau and Delbegetei) that occur among metasedimen-tary and metavolcanic rocks in the central part of Eastern Kazakhstan have a complex structure. They are as large as 100 to 300 km2 and isometric in plan view. The best documented Preobrazhenka intrusion (Fig. 6) comprises both mafic and granitic lithologies: (i) dolerite
(Ol+OPx+CPx+Pl+Bt), biotite gabbro (Pl+CPx+Bt±Amp), and monzodiorite (Pl+Amp+Bt±CPx) and (ii) Qtz monzonite (Pl+Kfs+OPx+Amp+Bt+Qtz), granosyenite (Pl+Kfs+Qtz+Amp+Bt), granite (Qtz+Pl+Kfs+Bt+Amp) and leucogranite (Qtz+Pl+Kfs±Bt±Grt) lithologies, respectively. The rocks of the two groups formed separately by differentiation of mafic and granitic parent magmas, which intruded synchronously, as evidenced by the presence of mingling structures (Fig. 6, b-d) [Khromykh et al., 2017a, 2018]. The Preobrazhenka intrusion was dated at 290±2 Ma (LA-ICP-MS zircon U-Pb, Qtz monzonite) and 290±1 Ma (LA-ICP-MS zircon U-Pb, granite) (Fig. 6, e-f). The Tastau granodiorites and granosyenites have LA-ICP-MS zircon U-Pb ages of 289±2 and 280±1 Ma, respectively [Khromykh et al., 2018].
The Preobrazhenka mafic and granitic rocks have independent composition trends in binary diagrams
0.054
0.050
0.046
0.042
EQtz monzonite
□ granite
Concordia Age = 290.7+1.8 Ma (2s, decay-const, errs included) MSWD (of concordance) = 1.4
0.15
0.25 0.35 '"РЬГи
0.45 0.55
0.049
0.047
0.045
Concordia Age = 290.4±1.3 Ma (2s, decay-const, errs included) .MSWD (of concordance) = 0.31
.16 0.20 0.24 0.28 0.32 0.36 0.40 0.44 ^РЫи
Fig. 6. (a) - simplified geology of the Preobrazhenka gabbro-granite intrusion [Khromykh et al., 2017a, 2018]. Blue circles mark mingling relations between granosyenite (phase 3) and monzodiorite (phase 4). (b-d) - photographs illustrating relationships between igneous rocks: monzodiorite (dark gray) and porphyritic granosyenite (light gray) nodules in granite of phase 3 (b); contact of monzodiorite and porphyritic granosyenite in an outcrop photo (c) and in the photo of a sample (d); U-Pb ages of Qtz monzonite of phase 1 (e) and granite of phase 3 f).
Рис. 6. (а) - схема геологического строения Преображенского габбро-гранитного массива [Khromykh et a¡., 2017a, 2018]. Голубыми кружками отмечены места проявления минглинг-взаимоотношений между граносиенитами 3-й фазы и монцодиоритами 4-й фазы. (Ь-С) - фотографии, иллюстрирующие взаимоотношения магматических пород: нодули монцодиоритов (темно-серые) и порфировидных граносиенитов (светло-серые) в гранитах 3-й фазы (Ь); контакт монцодиоритов и порфировидных граносиенитов в обнажении (с) и на срезе образца (с/); и-РЬ диаграммы с конкордией для цирконов из кварцевых монцонитов 1-й фазы (е) и из гранитов 3-й фазы (/).
Fig. 7. Composition of the mafic (dolerite and gabbro), felsic (Qtz monzonite, granosyenite and granite) and hybrid (monzodiorite) rocks from the Preobrazhenka intrusion.
I Рис. 7. Состав базитовых (долериты и габбро), кислых (Кв монцониты, граносиениты и граниты) и гибридных (монцодиориты) пород из Преображенского массива.
(Fig. 7) and show distinct dissimilarity in the contents of Al2O3, MgO, CaO and Rb, Ba, Zr, La, and Eu. Mafic subalkaline rocks have high alkali contents, with K2O up to 2 wt. % in gabbro and 2.5 wt. % in diorite, LREE higher than HREE, and relatively high Ba, K, Ti, Zr, and Sr. Granitic rocks are likewise rather rich in alkalis (3 to 6 wt % K2O); the contents of A^3, FeO, T1O2, MgO, CaO, Ba, Sr, and Eu decrease progressively from monzonite to granite and leucogranite.
The detailed petrological studies of the Preobra-zhenka rocks showed that mafic lithologies were derived from trachybasaltic magma by fractionation and contamination with crustal anatectic melts, while the
granitic lithologies result from melting of the lower or middle crust under a thermal impact of hot mafic magma. The origin of the intrusion was explained [Khromykh et al., 2018] in the context of interaction between mafic magma and granitic anatectic melts at different depths. This interaction led to reciprocal contamination of the mafic and felsic magmas and formation of Qtz-bearing monzogabbro and Qtz monzo-nite at the lower-crust level, but mingling structures formed at the middle-crust level where chemical mixing was minor; in the upper crust, mafic magmas did not interact with granitic material and formed a few dikes only.
82° E
50 km
early-batholith dikes of granodiorites and plagiogranites (P,)
post-batholith dike belts (279-267 Ma): felsic (1 ) and mafic (2) rocks
faults
Cenozoic sediments
Fig. 8. Simplified geology of the Kalba-Narym batholith, and the results of U-Pb (black squares) and Ar-Ar (white squares) isotopic dating [Kotler et al., 2015; Khromykh et al., 2016]. Inset shows the U-Pb ages of granitic samples of suites 1 and 2.
Рис. 8. Упрощенная схема строения Калба-Нарымского батолита и результаты изотопного датирования, выполненного U-Pb (черные прямоугольники) и Ar-Ar (белые прямоугольники) методами [Kotler et al., 2015; Khromykh et al., 2016]. На врезке - распределение U-Pb возрастов для образцов гранитов из 1-й и 2-й ассоциаций.
6. Large granitoid batholiths (295-275 Ma)
Remelting of the clastic metasedimentary and meta-morphic rocks led to the formation of two large granitoid batholiths in Eastern Kazakhstan: Zharma in the west, and Kalba-Narym in the east (see Fig. 2). The Kal-ba-Narym batholith extends from NW to SE within the Kalba-Narym turbidite terrane. According to a classical interpretation [Lopatnikov et al., 1982; Shcherba et al., 1998], it would be of collisional origin and would form during an orogenic stage, while the respective plutonic event would last 50-60 myr from the C3-P1 boundary to the P2-T1 boundary. However, new petrological and geo-chronological data [Kotler et al., 2015; Khromykh et al., 2016] show (Fig. 8) a shorter duration (20-25 myr, i.e.
from 300-295 to 280-275 Ma, Pi) and post-orogenic origin of the plutonism. The Kalba-Narym batholith consists of (1) an S-type granodiorite-granite suite making up most of the batholith volume, which emplaced in two phases at 296-288 Ma and 286-285 Ma, and (2) an A-type leucogranite-granite suite occurring as several large independent intrusions (283-276 Ma).
Suite 1 granodiorites and granites vary in SiO2 from 64 to 75 wt %, and all elements except K2O decrease with increasing silica contents (Fig. 9), which is common to S-type granites. The leucogranite-granite suite (2) shows a narrower SiO2 range of 73-76 wt. % and enrichment in Fe, REE, and HFSE (Ta, Nb, Zr, Hf) with silica increase (Fig. 9), as well as elevated contents of F and Li, which is closer to A-type granite compositions.
1 65 1 1 70 75
• ■ La ■ ■у
■ ■ ■ ■
• • с * ■. 1
••
I Fig. 9. Composition of granodiorite-granite (red circles, grey arrows) and granite-leucogranite (green squares, white arrows) suites from the Kalba-Narym batholith in the binary diagrams.
I Рис. 9. Состав пород гранодиорит-гранитной (красные кружки, серые стрелки) и гранит-лейкогранитной (зеленые квадратики, белые стрелки) ассоциаций Калба-Нарымского батолита на бинарных диаграммах.
Suite 2 granites and leucogranites form large independent intrusions, and there is a small gap between suite 1 and suite 2. We suggest the origin of Suite 2 in a separate melting pulse. The sources and conditions of granitic magma generation for the two suites were inferred from their mineralogy and chemistry, with reference to the compositions of the sedimentary and metamorphic rocks in the region, as well as to the experimental data on melting of crust protoliths. The rocks of suite 1 (similar to S-type granites) formed by partial melting of mixed metapelitic and metabasaltic substrates. The leucogranites and granites of suite 2 (similar to A-type granites) originated by melting of metapelitic crust, with participation of juvenile fluids enriched in HSFE and REE which interacted with the metamorphic material during melting.
7. Rare-metal granite dikes and pegmatites
(290-285 MA)
Granitic pegmatites in the Kalba-Narym zone bear extensive rare-metal mineralization (Ta, Nb, Li, Be, Sn, W etc.). They occur as veins in granitic rocks of phase 1 of the granodiorite-granite suite. Their relative chronology is confirmed by 40Ar/39Ar isotopic dating: the ages obtained for 12 mica samples from pegmatites range from 292 to 285 Ma [Kotler et al., 2014]. Rare-metal pegmatites are similar to ongonite and rare-metal granite-porphyry that form two dike swarms near Ust-Kamenogorsk city (Fig. 10). The larger Chechek dike swarm comprises about 15 dikes, 2 to 5 m thick and hundreds of meters long [Sokolova et al., 2016]. The age of the dikes was determined as
Ages of micas from (C)
Fig. 10. (a) - map of rare-metal mineralization in the Kalba-Narym zone, after [Sokolova et al., 2016]; (b) - Ar-Ar age of on-gonite from the Chechek dike belt [Khromykh et al., 2014]; (c) - Ar-Ar ages of muscovite and lepidolite from the rare metal pegmatite deposits [Kotler et al., 2014].
Рис. 10. (а) - схема распространения редкометалльной минерализации в Калба-Нарымской зоне, по [Sokolova et al., 2016]; (b) - Ar-Ar возрастной спектр для мусковита из онгонита из Чечекского дайкового пояса [Khromykh et al., 2014]; (с) - результаты определения возраста Ar-Ar методом для мусковита и лепидолита из редкометалльных пегматитовых месторождений [Kotler et al., 2014].
286±3 Ma by Ar-Ar dating of liquidus muscovite phe-nocrysts from a thick ongonite dike [Khromykh et al., 2014]. The dike rocks have high concentrations of LILE and F, like Li-F granites, and split into three composition groups with relatively high, high, and ultra-high contents of rare metals: (1) up to 1000 ppm Li+Rb+Cs, 0.45 wt % F, and 40-100 ppm IREE; (2) up to 2500 ppm Li+Rb+Cs, 1.4 wt. % F, 0.35 wt. % P2O5, and 3-15 ppm IREE; and (3) up to 4000 ppm Li+Rb+Cs and 110180 ppm IREE (Fig. 11). The concentrations of 'typical granitic' rare metals (Sn, Nb, Ta) in dikes are much higher than in granites (15-100 times more Sn, 1.5-2 times more Nb, and 2-12 times more Ta).
The mineralogy and chemistry of the dike rocks [Sokolova et al., 2016] suggests their origin from granitic melts that were enriched in rare metals. This makes them closer to rare-metal granite pegmatites of the Kalba-Narym batholith. We assume that magmas rich in rare metals formed in the granite chambers of the Kalba-Narym batholith. However, their local occurrence indicates that their generation involved
inputs of F, P2O5, rare metals, as well as other specific components with juvenile fluids, besides intra-chamber differentiation. This formation mechanism of the rare metal magmas is similar to that for suite 2 granites and leucogranites in the Kalba-Narym batholith.
8. Mafic dike swarms (280-270 Ma)
The juvenile fluids that contributed to the formation of rare metal granitic magmas may come from a sub-crustal mafic reservoir (magmatic underplating). Mafic magmatism in the Kalba-Narym zone occurs as dike swarms of the Myrolyubovka complex that intrude all granitic rocks (see Figs. 2 and 8), about 10 dike swarms, with 3-4 to 15-20 dikes in each unit. All dikes strike in the NE direction and are up to 4-5 meter thick and 2-3 km long. The dikes of the complex are mostly mafic though some have other compositions. The rocks are subalkaline and belong to high-K calc-alkaline series, have low contents of magnesium (Mg# ~39 %),
2.0-1
1.5-
1.0-
0.5-
+Rb+Cs), ppm
100.
10.
1.
0.1.
rock / chondrite
1000 2000 □ rare-metal type
3000 4000 5000 high rare-metal type
6000
La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
ultra-high rare-metal type
compositions of rare-metal granitoids of world
Fig. 11. Composition features of ongonites from Chechek and Akhmirovka dike belts [Sokolova et al., 2016].
Рис. 11. Особенности состава онгонитов из Чечекского и Ахмировского дайковых поясов [Sokolova et al., 2016].
and high TiO2 (~1.6 wt %), K2O (~1.7 wt %), P2O5 (~0.6 wt. %) and REE (sum ~195 ppm, Fig. 12, a-d). In addition, they contain greater concentrations of rare metals, fluorine and boron than the Kalba-Narym granitic rocks: 3-7 ppm Li, 0.9-3.5 ppm Cs, 16-38 ppm Rb, 0.4-0.8 ppm Sn, 0.1-0.5 ppm Be, 2-16 ppm Nb, 0.7-1.1 ppm Ta, 120-140 ppm F, and 1-3 ppm B. Therefore, the dike mafic rocks are derived from the mantle magmas that were the source of metals for the rare-metal granitic magmas. The available age constraints are LA-ICP-MS zircon U-Pb dates of 279±3 Ma for dolerite of the Manat dike and 267±1 Ma for spes-sartite of the Monastery dike (Fig. 12, e-f).
9. Correlation of magmatic events and mechanisms
OF PLUME-LITHOSPHERE INTERACTION
Thus, voluminous mantle and crustal magmatism affected the whole Eastern Kazakhstan in the interval of 300-270 Ma (Fig. 13, a). The rocks of mantle origin are enriched in alkalis, phosphorus, titanium and incompatible elements notably different from the older accre-tionary mafic-ultramafic complexes with subduction signatures [Safonova et al., 2012, 2018]. The appearance of enriched mantle magmas at the post-orogenic stage usually indicates their deeper sources. There are also assumptions that the appearance of enriched mantle magmas may be caused by remelting of meta-somatised mantle wedges [Konopelko et al., 2017]. Anyway, melting of the mantle indicates an increasing thermal gradient. The high thermal gradients most likely resulted from the activity of the Tarim mantle plume
which produced the early Permian Tarim LIP [Ernst, 2014; Gao et al., 2014; Wei et al., 2014; Xu et al., 2014; Yarmolyuk et al., 2014; Yu et al., 2017]. Based on the reported data, we infer that the Tarim LIP extends to the north, into the region of Eastern Kazakhstan (Fig. 13, b). The far-reaching influence of the Tarim LIP may have been facilitated by post-orogenic lithospheric extension [Buslov, 2011] after the Siberia-Kazakhstan collision. The extension led to rheological weakening of the lithosphere, whereby deep mantle melts could intrude into the sublithospheric mantle. The style of the mantle-crust interaction varied over the region depending on the permeability of the lithospheric blocks [Khromykh et al., 2017b]. In the central part of the region (see Fig. 2), where the fragments of accretionary and paleooceanic complexes still exist, mafic magmas could easily penetrate into the lower crust through the quite thin lithosphere. This may lead to intensive interactions of the mafic magmas with the crustal substrates and anatectic melts, forming the gabbro-monzonite-granite intrusions with a wide spectrum of rocks and mingling and mixing processes, and the appearance of syn-plutonic Mafic Microgranular Enclaves (MME) and combined mafic-felsic dikes [Wiebe, 1973; Furman, Spera, 1985; Litvinovsky et al., 1995; Barbarin, 2005; Renna et al., 2006; Burmakina, Tsygankov, 2013; Burmakina et al., 2018] In the northeastern part of the territory, clastic sediments (sandstones and silt-stones) deposited in the Devonian-Early Carboniferous within the Kalba-Narym terrane were deformed and metamorphosed in the course of collisional processes, and then were molten anatectically at high temperature gradients across the mantle chambers. Mafic
Na20+Kj0, wt. %
15-
10-
TAS [Middlemost, 1994\
1000
20-
10-
Zr/Y
2-
Island Arc/ Basalts/'
Zr-Zr/Y [Pearce, Norry, 1979]
Эо°
О О
/--------------—,
/ Mid-Ocean Ridge Basalts
(b)
Within-Plate Basalts
Zr, ppm
90 10 1000
20
50
100
200
500
1000
100-
100-
10-
~i-1-1-1-1-1-1-1-1-1-1-г
La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
CsRb^Th U К та NbLaCeSrNd Hf ZrSmEuGdTbDy Ti YErYb|_u
0.046
0.044
0.042
0.044
0.043
0.042
0.041
0.25 0.27 0.29 0.31 0.33 0.35 0.37 0.26 0.28 0.30 0.32 0.34
Fig. 12. Mafic rocks of the Mirolyubovka dike belts on the TAS (a) and Zr-Zr/Y (b) diagrams, and their REE (c) and trace-element (d) compositions; U-Pb ages of dolerite from the Manat dike (e) and spessartite from the Monastery dike (f).
Рис. 12. Составы базитовых пород миролюбовского комплекса на классификационных диаграммах TAS (а) и Zr-Zr/Y (b); спектры распределения РЗЭ (с) и мультиэлементные спектры (d) для базитовых пород; U-Pb диаграммы с конкордией для цирконов из долеритов дайки Манат (e) и из спессартитов дайки в Монастырском массиве f).
310 306 302 298 294 290 286 282 278 274 270 266 262
Age, Ma
Fig. 13. (a) - age histograms of the post-orogenic magmatic complexes from the Eastern Kazakhstan; (b) - the proposed boundaries of the Tarim Large Igneous Province taking into account the new data on magmatism of Eastern Kazakhstan.
Рис. 13. (a) - гистограмма возрастов, полученных для посторогенных магматических комплексов Восточного Казахстана; (b) - предполагаемые границы распространения Таримской крупной изверженной провинции с учетом новых данные по магматизму Восточного Казахстана.
magmas could not penetrate through thick viscous migmatite-granite lenses ('density filter') [Huppert, Sparks, 1988]. This mechanism includes interaction of the juvenile mantle fluids with the crust or with granitic magma in the chambers, as well as the inputs of some
elements responsible for rare-metal mineralization in granites [Abramov, 2004; Annikova et al., 2006; Zagorsky et al., 2014; Sokolova et al., 2016]. Thus, we revealed two main types of mantle-crust interaction: (1) direct interaction of mantle magmas with crustal material and ana-
94
I
tectic melts that produced large gabbro-granite intrusions, volcanic structures, and numerous small gabbro-picrite intrusions in central part of studied region; and (2) the effects of mantle heat and fluids on the crust. The intrusion of the mafic magmas into the middle and upper crust became possible only after large-scale granitoid magmatism had completed and the lithosphere had cooled down and deformed. This led to the formation of the Mirolyubovka dike swarms.
Thus, the early Permian history of Eastern Kazakhstan was controlled by the interplay of the plate tectonic and plume processes: plate-tectonic accretion and collision formed the structural framework, and the Tarim mantle plume provided a heat source to maintain voluminous magmatism.
10. Acknowledgements
We wish to thank Richard Ernst, Nikolai Dobretsov and Boris D'yachkov for fruitful discussions and valuable advice. Thanks are extended to Erzhan Sapargaliev for his assistance in the field and to Inna Safonova and Tatiana Perepelova for their help in manuscript preparation. This study was conducted according to the state assignment of IGM SB RAS. It was also supported by the Ministry of Science and Higher Education of the Russian Federation (Projects no. 5.1688.2017/4.6 and 14.Y26.31.0018) and the Russian Foundation for Basic Research (Projects no. 16-35-00209, and 17-05-00825).
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INFORMATION ABOUT AUTHORS | СВЕДЕНИЯ ОБ АВТОРАХ
Sergei V. Khromykh
Candidate of Geology and Mineralogy, Senior Researcher
V.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of RAS 3 Academician Koptyug ave, Novosibirsk 630090, Russia
Novosibirsk State University 2 Pirogov street, Novosibirsk 630090, Russia
e-mail: [email protected] © https://orcid.org/0000-0001-5951-0660
Сергей Владимирович Хромых
канд. геол.-мин. наук, с.н.с.
Институт геологии и минералогии им. В.С. Соболева СО РАН 630090, Новосибирск, просп. Академика Коптюга, 3, Россия
Новосибирский национальный исследовательский государственный университет
630090, Новосибирск, ул. Пирогова, 2, Россия
Pavel D. Kotler
Candidate of Geology and Mineralogy, Junior Researcher
V.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of RAS 3 Academician Koptyug ave, Novosibirsk 630090, Russia
Novosibirsk State University 2 Pirogov street, Novosibirsk 630090, Russia
e-mail: [email protected] © https://orcid.org/0000-0002-9654-6889
Павел Дмитриевич Котлер
канд. геол.-мин. наук, м.н.с.
Институт геологии и минералогии им. В.С. Соболева СО РАН 630090, Новосибирск, просп. Академика Коптюга, 3, Россия
Новосибирский национальный исследовательский государственный университет
630090, Новосибирск, ул. Пирогова, 2, Россия
Andrey E. Izokh
Doctor of Geology and Mineralogy, Professor, Head of Laboratory
V.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of RAS 3 Academician Koptyug ave, Novosibirsk 630090, Russia
Novosibirsk State University 2 Pirogov street, Novosibirsk 630090, Russia
e-mail: [email protected]
Андрей Эмильевич Изох
докт. геол.-мин. наук, профессор, заведующий лабораторией
Институт геологии и минералогии им. В.С. Соболева СО РАН 630090, Новосибирск, просп. Академика Коптюга, 3, Россия
Новосибирский национальный исследовательский государственный университет
630090, Новосибирск, ул. Пирогова, 2, Россия
Nikolai N. Kruk
Doctor of Geology and Mineralogy, Director of the Institute
V.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of RAS 3 Academician Koptyug ave, Novosibirsk 630090, Russia
Николай Николаевич Крук
докт. геол.-мин. наук, директор института
Институт геологии и минералогии им. В.С. Соболева СО РАН 630090, Новосибирск, просп. Академика Коптюга, 3, Россия
e-mail: [email protected]
