Application of magnesium stable isotopes for studying important geological processes—a review

doi:10.13745/j.esf.sf.2022.10.46

Abstract

Abstract:

Magnesium (Mg) is the fourth most abundant major rock-forming element on Earth (after O, Fe and Si). It has three naturally occurring stable isotopes, ²⁴Mg, ²⁵Mg and ²⁶Mg, among them the relative atomic mass difference between ²⁶Mg and ²⁴Mg is up to 8.33%. Such a large relative atomic mass difference can result in variable degrees of Mg isotope fractionation in different geological processes, thus making Mg stable isotopes effective tracers for studying various geological evolution processes. In recent years, improvements of isotope analytical methods and the development of isotope-ratio mass spectrometry have greatly expanded the use of Mg stable isotopes in geological research, and the related publications have been comprehensively reviewed. Here, following a brief introduction to the reference materials and analytical methods for Mg isotope analysis, this paper discusses in detail the application of Mg isotope in four geological research fields, including applications 1) in ore genesis studies as effective tracers for probing mineralization processes and source of ore-forming materials; 2) in lamprophyre genesis studies for compositional analysis of source materials; 3) in geothermometer research, where four common mineral-pair Mg isotope geothermometers are reviewed and their applicability analyzed; and 4) in the study of Mg isotopic fractionation during metamorphic evolution, peritectic reaction and magmatic processes involving garnet-bearing rocks, and its implications. This systematic review is aimed to deepen the understanding of Mg stable isotopes and further demonstrate their broad application prospects.

Key words: Mg isotopes, analytical method, ore genesis, lamprophyre genesis, geological geothermometer, metamorphic magmatic process

CLC Number:

P597.2

LIU Jiawen, TIAN Shihong, WANG Ling. Application of magnesium stable isotopes for studying important geological processes—a review[J]. Earth Science Frontiers, 2023, 30(3): 399-424.

Figures/Tables 16

Fig.1 Mg isotopic compositions of various natural reservoirs. The vertical dashed line represents the average δ26Mg value of (-0.25±0.07)‰ for the mantle. Modified after [4,6,11,36⇓⇓⇓-40].

Table 1 Comparison of four analytical methods for Mg isotope

分析方法		化学前处理	精度(2SD)	空间分辨率	干扰校正方法	参考文献
溶液法	TIMS	是	1‰~2‰			[17-18,45-46]
溶液法	MC-ICP- MS	是	0.03‰~0.14‰		SSB和DS校正仪器质量分馏、膜去溶进样去除(C₂₊、CN⁺等)原子离子干扰、优化化学纯化流程去除基质效应	[10,45⇓⇓⇓⇓-50]
原位法	LA-MC- ICP-MS	否	0.11‰~0.15‰	50~200 μm	SSB校正仪器质量分馏、调整激光束斑等激光剥蚀条件以减少分馏效应、提高仪器的分辨率去除⁴⁸Ca²⁺同质异位素的干扰	[10,48-49,51-52]
原位法	SIMS	否	0.2‰	10~20 μm	传输过程优化、高分辨率去除同质异位素干扰	[48]

Fig.2 δ26Mg value distribution plot for dolomite and carbonatite from the Bayan Obo deposit. Modified after [81].

Fig.3 Plots of εNd(t) vs. (87Sr/86Sr)i (a), εNd(t) vs. δ26Mg (b) and (87Sr/86Sr)i vs. δ26Mg (c) for peridotites and marbles from the Jinchuan magmatic sulfide deposit for ore genetic study. Modified after [33].

Fig.4 δ26Mg vs. δ41K plot for altered samples from the Dexing porphyry deposit for the identification of thermal fluid types. Grey shadows represent δ26Mg and δ41K baseline values for igneous rock. Modified after [35].

Fig.5 Plots of δ26Mg vs. CaO/Al2O3 (a), Hf/Hf* (b), Ti/Ti* (c), 87Sr/86Sr (d), 143Nd/144Nd (e) and 206Pb/204Pb (f) for the Leucite Hills lamproites for lamporphyre genetic study. Modified after [39].

Fig.6 Simplified cartoon describing two metasomatic events in modifying the lithospheric mantle sources of the Leucite Hills lamproites. Modified after [39].

Fig.7 δ26Mg versus CaO/Al2O3 (a), Fe/Mn (b) and Ti/Ti* (c) for the Ailaoshan lamprophyres. Modified after [116].

Fig.8 Mg-Sr isotope binary mixing model for the Ailaoshan lamprophyres. Modified after [116].

Fig.9 Mg-Sr isotope ternary mixing model. Modified after [125].

Fig.10 δ26Mg versus MgO (a), CaO/Al2O3 (b), (87Sr/86Sr)i (c) and 143Nd/144Nd (d) for the Shandong lamprophyres. Modified after [40].

Fig.11 δ26Mg value distribution of different minerals. Modified after [4,135].

Fig.12 Comparison of expression formulas between biotite-garnet Mg isotope geothermometer and garnet-clinopyroxene Mg isotope geothermometer. Modified after [156]. Black solid line is an empirical equilibrium fractionation equation of Δ26MgCpx-Grt=0.83×106/T2 from [148]; Blue solid line is also an empirical equilibrium fractionation equation of Δ26MgCpx-Grt=0.86×106/T2 from [149]; Red solid line and dotted line represent the theoretically determined equilibrium fractionation equations of Δ26MgCpx-Grt=f1(p)×(106/T2) + f2(p)×(106/T2)2 + f3(p)×(106/T2)3 from [150]; Purple circle is an empirical equilibrium fractionation equation of Δ26MgBt-Grt=0.96×106/T2 from [156].

Fig.13 H2O versus MgO for the greenschists, amphibolites and eclogites. Modified after [181].

Fig.14 δ26Mg versus Zr/Hf (a), K/Rb (b), Eu/Eu* (c) and 1/TiO2 (d) for the Himalayan leucogranites. Modified after [190].

Fig.15 δ26Mg values versus degree of partial melting of melt and residual of garnet peridotite and garnet pyroxenite. Modified after [160,191].

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