Zircon from the economic ultramafic-mafic Kharaelakh
intrusion (Russia): first U-Pb and Hf-isotope constraints on timing and source composition
Malitch K.N.*, Griffin W.L.**, Badanina I.Yu.*,
Petrov O.V.*, Tuganova
E.V.*, Belousova E.A.**, Pearson N.J.**, Knauf V.V.***, Presnyakov S.L.*
* A.P. Karpinsky
Russian Geological Research Institute (VSEGEI), St. Petersburg, Russia; ** GEMOC ARC National Key Centre, Department of Earth and Planetary
Sciences, Macquarie University, Sydney, Australia; *** NATI Research JSC, St. Petersburg, Russia
Introduction. World-class
PGE-Cu-Ni sulphide deposits occur in the Noril’sk-1, Talnakh and Kharaelakh areas in
the northwestern part of the Eastern Siberia, Russia. They are associated with
sill-like ultramafic-mafic intrusions, which are
controlled by a long-lived intracontinental paleorift (Tuganova,
2000). These ‘Noril’sk-type’ intrusions range in
thickness up to 360 m and in length up to 25 km. In this study, we present new
U-Pb and Hf-isotope data
for 23 zircon grains from the Kharaelakh intrusion in
order to: (1) provide age constraints on the magmatic
evolution and (2) specify the sources of materials involved in the generation
of the host rocks.
Samples and analytical methods. A distinctive feature of the Kharaelakh intrusion is the presence of two horizons of ultramafic rocks, distinguishing this intrusion from the Talnakh and Noril’sk-1 intrusive bodies. The rocks
investigated comprise (from top to bottom) olivine gabbro
(samples 844-1, 844-6), plagiowehrlite (844-7) and melanotroctolite (844-10,11). Forty
grains of zircon were extracted using a ppm-mineralogy
technique at NATI Research JSC (Russia). Grains of zircons were hand picked
from each concentrate, imaged by SEM and subsequently mounted in epoxy blocks
together with grains of the TEMORA and 91500 reference zircons. Transmitted and
reflected light photomicrographs and cathodeluminescence
images were made in order to select grains and choose sites for analyses,
avoiding cracks and inclusions. The Sensitive High-Resolution Ion Microprobe
(SHRIMP-II) at the VSEGEI was used to perform 26 in-situ U-Pb analyses by applying a secondary electron multiplier in
a peak-jumping mode following the procedure described by Williams (1998).
Age calculations use the routines of Ludwig (2003) and follow the decay
constant recommendations of Steiger and Jager (1977). In-situ
Hf-isotope data were collected on the dated spots
within zircon grains. Twenty-six Hf-isotope analyses
were carried out with a New Wave LUV213 laser-ablation microprobe attached to a
Nu plasma MC-ICP-MS at GEMOC, following the analytical procedures reported by Griffin
et al. (2002). The measured 176Lu/177Hf ratios and
the 176Lu decay constant of 1.865x10-11 yr-1
reported by Scherer et al. (2001) were used to calculate initial 176Hf/177Hf
ratios. The present-day chondritic values of 176Lu/177Hf=0.0332
and 176Hf/177Hf=0.282772 reported by Blichert-Toft
and Albarede (1997) were used for the
calculation of epsilon Hf values (parts in 104
difference of initial Hf isotope ratios between the
zircon sample and the chondritic uniform reservoir).
Morphology and internal structure. Zircon has been observed in thin sections as
single grains or aggregates enclosed in clinopyroxene,
amphibole or mica, frequently intergrown with
apatite. Separated zircon grains are commonly idiomorphic to subidiomorphic prismatic, transparent to semi-transparent,
light beige crystals that may contain fissures; the elongation of zircon grains
varies from one to three (sometimes up to 6-7). In the Pupin diagram (Pupin,
1980), type D crystals predominate (76 %) among the investigated grains,
indicative of alkaline-high temperature conditions of formation. Observations
under the petrographic microscope revealed distinct
zircon populations with different internal structure. However, zircons are
characterized by similar fuzzy cathodeluminescence, commonly with a total absence of the growth zoning typical
of zircons from magmatic rocks.
U-Pb ages. Twenty-three zircon grains used for the U-Pb determinations yielded four groups of concordant U-Pb ages. Colorless cores from complex grains 844-1_10 and
844-1_7, defined as population 1 (ZR 1), produced a 206Pb/238U
age of 347 ± 16 Ma (mean square of
weighted deviates (MSWD) = 1.2), which is significantly older than ages found
in the other types.
Indeed, rims of zircons from these complex
grains (population 2, ZR 2) gave a 206Pb/238U
age of 265 ± 11 Ma (MSWD=2.3), whereas
dark cores from two other complex grains (i.e., 844-1_19 and 844-6_28) and the
main set of homogeneous grains (n=15) yielded slightly younger concordant 206Pb/238U age
of 253.8 ± 1.7 Ma, MSWD=0.064). A younger concordant 206Pb/238U
age of 235.7 ± 6.1 Ma (MSWD=2.0) is
typical of overgrowths
over dark cores and a minor group of homogeneous grains. For consistency, we
refer to the groups of zircon with 206Pb/238U ages of
253.8 ± 1.7 and 235.7 ± 6.1 as population 3 (ZR 3)
and population 4 (ZR 4), respectively.
Hf-isotope
data. The studied
zircons show a wide range in Hf-isotope composition.
Zircons of population 1, represented by colorless cores in complex
grains with 206Pb/238U ages between ca 338-355 Ma, yielded eHf (parts in 104 deviation of initial Hf isotope ratios between the zircon sample and the chondritic uniform reservoir) values from + 8.1 to + 8.7
(mean eHf + 8.4). Zircons of population 2
with 206Pb/238U ages between ca. 264.9-270 Ma (exemplified by
rims from the same complex grains) have Hf isotope
compositions that are less radiogenic than the other zircon populations (e.g. ZR1,
ZR 3 and ZR 4). Population 3 zircons with 206Pb/238U
ages between ca. 241.8-267.2 Ma and population
4 zircons with 206Pb/238U ages between ca.
229.4-239.6 Ma have similar mean eHf values (10.5 and 9.95,
respectively), which are only slightly higher than that of type 1.
However, populations 3 and 4 zircons show a
significant range in eHf (from +5.1 to +16.7 and + 4.9 to +13.1,
respectively) with some points plotting close to the Depleted Mantle reference
line, while the least radiogenic points fall close to the values observed in ZR 2.
Genetic implications and concluding remarks. The U-Pb
ages of the four zircon populations cover a significant time span (347 ± 16, 265 ± 11, 253.8 ± 1.7 and 235.7 ± 6.1 Ma) suggesting a prolonged evolution
of the magmatic system. This magmatic
activity is consistent with two recognised stages of
active tectonism in the development of the Siberian Craton (Malitch,
1975). The crystallisation of zircon population 1
corresponds to the final stages of the Middle Paleozoic (D3-C1)
tectonic cycle, whereas that of populations 2 to 4 matches the known duration
of the Early Mesozoic (P2-T2) tectonic event.
On the basis of results reported
here we propose that mafic-ultramafic magmas were
emplaced in the lithospheric mantle or deep crust ca
90 Ma before the flood basalts, and that the magmas generated in Early Mesozoic
(around 230-260 Ma) picked up zircons from these earlier intrusions. We also
suggest that this might represent a single long-lived magma chamber. The age of
zircon population 3 (253.8±1.7 Ma)
slightly precedes that suggested for the basalts (248.7±0.6 – 250.3.2±1.1 Ma, Reichow et al., 2009). Therefore, the timing of the magmatic episode exemplified by ZR 3 might be closely linked and possibly interpreted as coeval
with flood-basalt volcanism. ZR 4 can be attributed to thermal recrystallisation
during or after the emplacement of the intrusion, clearly postdating the
eruption of the basalts.
Hf isotope data show that majority of
studied zircons have a clear juvenile component, and there is good evidence of
mixing with an older, possibly lithospheric component.
The Hf-isotope data for zircons of population
3 suggest that the Kharaelakh magmas represent mixing
between a juvenile source equivalent to the Depleted Mantle, and a lithospheric source with Hf-isotope
composition similar to the zircons of population 2. The smaller range of
initial 176Hf/177Hf values in population 4 might reflect progressive homogenization of these
magmas during crystallisation, but the present
dataset is too small to say this with confidence.
The depleted mantle component was
not previously recognised by whole-rock Nd- and Sr-isotope studies (Arndt
et al., 2003, among others). All rocks at Kharaelakh
from which zircons were separated are characterised
by eNd values from + 0.8 to + 1.1. However, the existence of a highly depleted
mantle source (eNd in the
range of +3.7 and +5.1) has been confirmed (Kogarko
et al., 1988; Horan et al., 1995) in picritic
lavas, both at Noril’sk (Gudchihinsky
suite) and Maimecha-Kotui (Maimechian
suite) areas. Therefore, the slightly lower uniform Nd
isotopic values typical of ore-bearing ‘Noril’sk-type’
ultramafic-mafic intrusions were attributed to
certain levels of crustal contamination, presumably
in deep staging magma chambers. Our data confirm that a lithospheric component is present. The Sm-Nd
whole rock data reflect this (and the homogenising
effect of whole-rock analysis) more strongly, while the zircon data allow us to
put better constraints on the end-members of the mixing (DM vs
an old lithospheric component with eHf ≈ 0 at 250 Ma).
In conclusion, our new findings
suggest a prolonged period of mafic-ultramafic magmatic activity, from Middle Paleozoic to Early Mesozoic,
and interaction between juvenile magmas and an older lithospheric
component, at least during the ca 253 Ma magmatism.
Consequently, these processes could lead to high degrees of separation and
concentration of ore elements and formation of specific ore magmas of unique
scales and concentrations. We further propose that ‘radiogenic’ Hf-isotope composition of zircon can be employed as an
effective fingerprint for identifying prospective intrusive host rocks and
consequently is useful in exploration for sulphide-rich
ores associated with ‘Noril’sk-type’ intrusions.
Finally, our new data suggest that the Hf-isotope
composition of defined zircon types can provide a unique set of previously
unknown constraints on petrologic history of the Kharaelakh
intrusion.
References
Arndt N.T., Czamanske G.K.,
Walker R.J., Chauvel C., Fedorenko
V.A. Geochemistry and
origin of the intrusive hosts of the Noril’sk-Talnakh
Cu-Ni-PGE sulfide deposits // Economic Geology. 2003. Vol. 98, P. 495-515.
Blichert-Toft J., Albarede F. The Lu-Hf isotope geochemistry of chondrites
and the evolution of the mantle-crust system // Earth and Planetary Science
Letters. 1997. Vol. 148. P. 243-258.
Griffin W.L., Wang X.,
Jackson S.E., Pearson N.J., O’Reilly S.Y., Xu X.,
Zhou X. Zircon
chemistry and magma genesis, SE China: in-situ analysis of Hf
isotopes, Pingtan and Tonglu
igneous complexes // Lithos. 2002. Vol. 61. P.
237-269.
Horan
M.F., Walker R.J., Fedorenko V.A., Czamanske G.K. Osmium and neodymium isotopic constraints on
the temporal and spatial evolution of Siberian flood basalts sources // Geochimica et Cosmochimica Acta. 1995. Vol. 59. P. 5159-5168.
Kogarko L.N., Karpenko S.F., Lyalikov
A.V., Teptelev M.P. Isotope criteria of the meimechite genesis // Doklady Academii Nauk SSSR. 1988. Vol. 301.
P. 939-942 (in Russian).
Ludwig K.R. User’s Manual for ISOPLOT/Ex 3.00. A Geochronological Toolkit for Microsoft
Excel. Berkeley Geochronology Center Special
Publication. 2003. No. 4. 70
pp.
Malitch N.S. Tectonic
evolution of the cover of the Siberian Craton. Moscow: Nedra
Press, 1975. 215 pp (in Russian).
Pupin J.P. Zircon and granite petrology
// Contributions to Mineralogy and Petrology. 1980. Vol. 73. P. 207-220.
Reichow M.K.,
Pringle M.S., Al’mukhamedov A.I., Allen M.B., Andreichev V.L., Buslov M.M.,
Davies C.E., Fedoseev G.S., Fitton
J.G., Inger S., Medvedev A.Ya., Mitchell C., Puchkov V.N.,
Safonova I.Yu., Scott R.A.,
Saunders A.D. The
timing and extent of the eruption of the Siberian Traps large igneous province:
Implications for the end-Permian environmental crisis // Earth and Planetary
Science Letters. 2009. Vol. 277. P. 9-20.
Scherer E., Munker C., Mezger K. Calibration of the lutenium-hafnium clock // Science. 2001. Vol. 293. P.
683-687.
Stieger R.H., Jager E. Subcommission on geochronology:
convention on the use of decay constants in geo- and cosmochronology
// Earth and Planetary Science Letters. 1977. Vol. 36. P. 359-362.
Tuganova E.V. Petrographic types, genesis and regularities of
distribution of PGE-Cu-Ni sulfide deposits. St. Petersburg: VSEGEI Press, 2002. 102 pp (in Russian).
Williams I.S. U-Th-Pb
Geochronology by Ion Microprobe // In: McKibbe M.A., Shanks W.C., Ridley W.I. (eds.) Applications of microanalytical techniques to understanding mineralizing
processes, Reviews in Economic Geology 1998. Vol. 7.
P. 1-35.