Study of the nature of magmatic complexes using NRE
ratio values
Volodkova T.V.
Yu. A. Kosygin Institute of Tectonics and Geophysics,
š
The major part of ore regions
of Priamurye is covered by aerogeophysical
survey (aeromagnetic prospecting, aerogammaspectrometry)
scale of 1:50000-1:10000, using complex aerogeophysical
station devices SKAT€77 an
STK-11. Measurement accuracy of the natural radioactive elements (NRE)
content attains to the following values: for uranium - (0.1-0.15)*10-4%,–for
thorium – (0.55-0.65)*10-4%, for potassium – (0.05-0.10)%.
Magmatic complexes are characterized by average background U/Th, K/Th, U/K ratio values; as compared
to NRE contents, these are less dependent on survey errors and are
commensurable with the results obtained by ground survey. The confidence level
values (±σ) attain to: U/Th – 0.1; K/Th – 0.1; U/K – 0.25.
In terms of
isotopic geology, uranium, thorium and potassium are a part of a group of
extremely incompatible elements-indicators of magmatic processes. Unaltered
rocks, formed due to processes of crystallization differentiation in closed
magma chambers are characterized by constant NRE ratios irrespective of the
composition. They are close in age, being related to the main stages of a
single magmatic cycle, which is comparable with the time of existence of magma
chamber. Hydrothermally-metasomatically altered rocks
(degree of alteration of more than 10-20 %) are distinguished by the anomalous
NRE ratios. In the open magma chambers conditions for crystallization vary from
phase to phase due to deep fluid inflow, therefore, the average NRE ratio
values will vary regularly for magmatic rocks. The background NRE ratio values
vary sharply for magmatic complexes due to affecting hydrothermal-metasomatic processes, mantle metasomatism
and geodynamic environments. It has been elaborated methodology taking into
consideration the influence of hydrothermal-metasomatic
processes on NRE ratio characteristics, such data are eliminated from sampling
when making statistical reports. The mantle metasomatism
and juvenile fluidization are typical of plume magmatism;
intrusion of exclusively subalkali and alkali rocks
is associated with it. In Priamurye magmatic rocks of
plume nature are associated with hot spot areas and the Maya-Selemdzha plume which are distinguished from
geological-geophysical data. The NRE ratio characteristics for subalkali rocks are weakly anomalous (weak fluid inflow);
these may reach “hurricane” values for alkali rocks (the Ingili,
Arbarastakh massifs).
Characteristics
of average NRE ratio values for normal granitoids in
different geodynamic environments.
Name
of intrusive (IC) and volcanic (VC) complexes*1 |
NRE
ratio values |
Notes*2 |
||
U/Th |
K/Th |
U/K |
||
Continental crust CC |
0.23 |
0.25 |
0.85 |
Nikolaeva, 1997; Ryabchikov,
1997 |
Sedimentary layer |
0.20 |
0.20 |
0.20 |
Smyslov, 1974 |
Granite-metamorphic layer |
0.25 |
0.20 |
1.28 |
Smyslov, 1974 |
Andesite-metamorphic layer |
0.21 |
0.21 |
1.00 |
Smyslov, 1974 |
Granulite-basic |
0.33 |
0.50 |
0.66 |
Smyslov, 1974 |
Primitive
mantle òí |
0.26 |
0.30 |
0.94 |
Ryabchikov,1997;
Flerov,2001 |
Depleted
mantle DM |
0.40 |
0.53 |
0.80 |
Ryabchikov, 1997; Khain, 2002 |
Enriched
mantle EM I |
0.08 |
0.17 |
0.45 |
Woodhead, 1989; Weaver, 1991 |
Enriched
mantle EM II |
0.49 |
0.49 |
1.00 |
Wilson,
2001; Weaver, 1991 |
Enriched
mantle HIMU |
0.25 |
0.10 |
2.51 |
Chauvel, 1992 |
Ultrabasic rocks |
0.37 |
1.7 |
0.20 |
Bazilevsky, 1985 |
Alaskite granites |
0.50 |
0.28 |
1.75 |
Bazilevsky, 1985 |
Meimechites, ijolites |
0.27 |
0.18 |
1.45 |
Bazilevsky, 1985 |
Nepheline agpaite
syenites |
0.36 |
0.18 |
2.04 |
Bazilevsky, 1985 |
Basalts,
trachydacites, J3-K1š |
0.33 |
0.57 |
0.80 |
Subalkali range, |
Plateaubasalts,
basalt-comendite-pantellerite associations, PZ3-MZ1 |
0.32 |
0.58 |
0.56 |
|
Alkali
basalts, source is close to DM, KZ1 |
0.25 |
1.01 |
0.20 |
|
Alkali
basalts, source is DM+HIMU, KZ1 |
0.23 |
0.48 |
1.10 |
|
Alkali
basalts, source is DM+EM, KZ1 |
0.33 |
0.90 |
0.63 |
|
Konder IC, ultrabasic
alkali rocks, PR1 |
0.45 |
0.25 |
1.3 |
Subalkali range, Konder massif, |
Quartz
subalkali diorites, K1 |
0.45 |
1.10 |
0.75 |
|
Granites,
porphyry-like monzodiorites, PZ1 |
1.05 |
0.80 |
1.15 |
Kalar massif, normal-subalkali range of Na-series |
Leucocratic
syenites, PZ1 |
1.25 |
0.50 |
0.85 |
|
Ingili
IC, alkali-ultrabasic rocks, PR3 |
0.28 |
0.08 |
4.75 |
Ingili and Arbarastakh
massifs, alkali range of K-Na series |
Arbarastakh IC,
alkali-ultrabasic rocks, PR3 |
0.82 |
0.13 |
15.0 |
|
Amphibole-bearing
calc-alkali granitoids of I-type |
0.25 |
0.14 |
1.73 |
|
Porphyry-like
biotite granites of I-type |
0.29 |
0.14 |
2.10 |
Tyrnauz, Rozen,
2001 |
Felsic rocks with decreased
alkalinity of subduction I-type |
0.40 |
0.30 |
1.90 |
The Kuriles, Volodkova,
2007 |
High
aluminous collisonal granitoids
of S -type |
0.26 |
0.18 |
1.47 |
|
Felsic calc-alkali island-arc
rocks of í-type |
0.20 |
0.30 |
0.65 |
The Kuriles, Volodkova,
2007 |
Monzonites of á-type |
0.11 |
0.17 |
0.66 |
Trans Baikal, Tsigankov, 2007 |
Quartz
syenites of A-type |
0.16 |
0.08 |
0.16 |
Trans Baikal, Tsigankov, 2007 |
The
U/K ratio can be used as a geodynamic criterion. Purely subduction
(Andean) amphibole-bearing biotite granitoids as well as those transitional to collisional (early collisional)
can be referred to I-type (U/K≥ 0.75). Taking into consideration the U/K
ratio value, one can refer calcareous plagiogranites,
the Kurile island arc granites to I-type. The category of collisional
granitoids of S-type (U/K=1.30-1.75) includes syncollisional and late collisional
granitoids; we can distinguish post-collisional and proper intraplate
ones among the magmatic rocks of á-type. The post-collisional
granitoids are characterized by U/K=0.75-1.30 values;
as for intraplate rocks with increased alkalinity,
associated with plume effect, U/K≤0.75 values are typical. Taking into
consideration the U/K ratio the island-arc granitoids
(the Kuriles), namely: quartz diorites, diorites,
calc-alkali gabbroids are referred to í-type. From
geophysical data, the Kurile subduction calcareous granitoids are associated with the crustal magma sources,
while those of í-type
–with the mantle ones being formed due to the Kurile mantle diapir
(plume) (Volodkova, 2008). Granitoids
formed due to the mantle sources, the intraplate
continental (A-type) and island-arc (M-type) ones, are not differentiated from
the U/K ratio criterion; for the granitoids of both
categories increased alkalinity is typical and the U/K ratio values are
significantly lower as compared to characteristics of depleted mantle. By all
appearances, both categories of granitoids are formed
due to the mantle metasomatism processes.
Geodynamic
types of magmatic rocks are determined by the processes occurring within the
lithosphere and asthenosphere; magmas of plume nature
reflect deeper physical-chemical conditions. The formation of EM I, EM II, HIMU
mantle reservoirs is related to the plume influence (Weaver, 1991); EM I and
HIMU reservoirs are contrastingly distinguished, while EM II one is close to
the crustal parameters according to NRE ratios. It is in consistency with the
well-known point of view on the formation of EM II from the continental crust
due to recycling.
Taking
into account the NRE ratio values, the magmatic complexes with increased
alkalinity are to either extent formed due to the following sources (Volodkova, 2008):
1.
EM I source (U/K <0.75);
2.
HIMU source (U/K >1.75);
3.
Rocks with intermediate
characteristics of NRE ratio of 1.25<U/K<1. 75 more rarely occur; they
are formed based on substrate with ingreased basicity, recycled by deep fluids;
4.
Probably, EM I and HIMU sources
characterize two mantle levels of different depth;
5.
Geodynamic types of magmatic rocks
are related to the plume processes and can be formed as follows: I-type –due to
HIMU mantle source, A-type – due to EM I mantle source.
References
1.
Volodkova
T.V. Characteristics of alkali rocks of Priamurye from
aerogammaspectrometry data // Alkali magmatism of the Earth.š
2.
Volodkova
T.V. Granites and Earths Evolution: geodynamic Position, Petrogenesis
and Ore Content of Granitoid Batholiths.
3.
šBarry L. Weaver. The origin of ocean island
basalt end-member compositions trace element and isotopic constraints // Earth
and Planetary Science Letters. 1991. Vol. 104. P.381-397.