Generalized Р—Т path and fluid regime of exhumation of metapelites of the central zone of the Limpopo complex, south Africa

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The P–T paths of exhumation of Precambrian granulite complexes at the craton boundaries usually include two stages: sub-isothermal decompression and a decompression–cooling stage with a more gentle P–T path. Our goal is to understand the possible causes of the change in the slope of the P–T path of exhumation of the Central Zone (CZ) of the Limpopo granulite complex (South Africa), located between the Kaapvaal and Zimbabwe cratons. For this purpose, rocks (mainly, metapelites) from various structural positions within the Central Zone, i.e. dome structures, regional crossfolds, local and regional shear-zones, were studied. Metapelites are gneisses of similar bulk composition. Relics of leucosomes composed of quartz-feldspar aggregates with garnet and biotite are variously manifested in rocks, and melanocratic areas enriched in cordierite usually mark micro-shear-zones that envelope and/or break garnet porphyroblasts. Study of polymineral (crystallized melt and fluid) inclusions in garnet, its zoning with respect to the major (Mg, Fe, Ca) and some trace (P, Cr, Sc) elements, fluid inclusions in quartz, as well as phase equilibria modeling (PERPLE_X) showed that rocks coexisted with granite melts and aqueous-carbonic-salt fluids (aH2O = 0.74–0.58) at the peak of metamorphism at 800–850°C and 10–11 kbar. Partial melting initiated sub-isothermal exhumation of rocks to 7.5–8 kbar during diapirism of granitic magmas in the Neoarchean (2.65–2.62 Ga). This is reflected in the specific zoning of garnet grains in terms of the grossular content. A change in the rheology of rocks as a result of partial removal and crystallization of the melt activated shear-zones during further exhumation to 6–5.5 kbar along the P–T decompression–cooling path of 95–100°/kbar, reflecting a slower uplift of rocks in the middle crust. This process was resumed due to thermal effects and interaction of rocks with aqueous fluids (aH2O > 0.85) in the Paleoproterozoic (~2.01 Ga). Such a scenario of metamorphic evolution implies that the Limpopo granulite complex, in general, and its Central Zone, in particular, are the result of the evolution of an ultra-hot orogen, where vertical tectonic movements associated with diapirism were conjugate with horizontal tectonic processes caused by the convergence of continental blocks.

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作者简介

O. Safonov

Korzhinskii Institute of Experimental Mineralogy, Russian Academy of Sciences; Lomonosov Moscow State University; University of Johannesburg

编辑信件的主要联系方式.
Email: oleg@iem.ac.ru

Faculty of Geology, Department of Geology

俄罗斯联邦, Chernogolovka, Moscow oblast; Moscow; Johannesburg, South Africa

V. Yapaskurt

Lomonosov Moscow State University

Email: oleg@iem.ac.ru

Faculty of Geology

俄罗斯联邦, Moscow

D. van Reenen

University of Johannesburg

Email: oleg@iem.ac.ru

Department of Geology

南非, Johannesburg

C. Smit

University of Johannesburg

Email: oleg@iem.ac.ru

Department of Geology

南非, Johannesburg

S. Ushakova

Lomonosov Moscow State University

Email: oleg@iem.ac.ru

Faculty of Geology

俄罗斯联邦, Moscow

M. Golunova

Korzhinskii Institute of Experimental Mineralogy, Russian Academy of Sciences

Email: oleg@iem.ac.ru
俄罗斯联邦, Chernogolovka, Moscow oblast

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2. Fig. 1. Map of the Limpopo complex located between the Kaapvaal and Zimbabwe cratons (van Reenen et al., 2019). The map shows the subdivision of the complex into the Northern Marginal Zone (SKZ), the Central Zone (ZZ) and the Southern Marginal Zone (SKZ), regional shear plastic deformations separating the zones from each other and from cratons, as well as the main components of the ZZ (Beit Bridge, Fikwe, Mahalapi complexes).

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3. Fig. 2. A schematic map showing the details of the geological structure of the eastern part of the Central Zone of the Limpopo complex, with the designation of the sampling sites of the studied samples (Table. 1) within the Ha-Tshanzi dome structure, the Campbell transverse fold, the Chipize deformation zone and the northern contact of Pluto Bulai.

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4. Fig. 3. Generalization of some published R–T trends in the metamorphic evolution of the Central zone of the Limpopo complex. The R–T trends drawn with dashed lines according to the data (Perchuk et al., 2008a; Brandt et al., 2018; Yang et al., 2023) correspond to the Paleoproterozoic stages of metamorphism.

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5. Fig. 4. Variations in the gross composition of the studied metapelites in the coordinates SiO2–(MgO + FeO)–Al2O3. The blue and light purple fields indicate the compositions of high-alumina and low–alumina metapelites of the Central Asian Region, respectively (Boryta, Condie, 1990; Rajesh et al., 2018a), the pink field indicates the compositions of leucocratic Singelele granites (Rajesh et al., 2018b). The green square is the average melt composition modeled for HT-HP group metapelites (see the text).

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6. Fig. 5. REE spectra (normalized to CI chondrite; McDonough, Sun, 1995) of some of the studied samples of TS metapelites. Gray field – REE spectra of high-alumina and low-alumina metapelites of Central Asia (Boryta, Condie, 1990). The yellow field is the REE spectra of Singelele leukocratic granitoids (Rajesh et al., 2018b).

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7. Fig. 6. Petrographic characteristics of the studied metapelite samples. (a) Crushed pomegranate grains bordered by microzones of deformations, model LP19-29. (b) Pomegranate grains, model LP19-14; in grains in quartz-feldspar bulk, nuclei filled with inclusions are surrounded by a symmetrical zone without inclusions; in grains partially surrounded by cordierite crowns, nuclei with inclusions are shifted to the edges and cut off by the bulk; sillimanite inclusions are present in the marginal zones of some grains. (c) Quartz feldspar lenses and their envelopes of deformation microzones, folded Crd + Bt + Sil + + Qz, mod. O6-19. (d) Garnet porphyroblast, broken by a microzone of deformation, mod. DOV-21. (e) Fragments of large porphyroblasts of garnet, united by a cordierite (+Bt + Sil + Pl + Qz) crown developed along a microzone of deformation, model LP19-21. (f) Xenomorphic grains of garnet surrounded by wide cordierite (+biotite) crowns, model LP19-12. (g) A Ca distribution map showing plagioclase secretions (light grains and borders) in the crowns around the pomegranate grain, mod. DOV-21; Pl1 – primary plagioclase, Pl2 – plagioclase in the crowns, which is a product of garnet decomposition. (h) Substitution of rutile with ilmenite in the cordierite corona around the garnet, mod. O6-19. (i) Rutile-carbonate-sulfide aggregates, model LP19-29. (k) Two generations of garnet, model LP19-08: large grains (Grt1) with numerous inclusions forming lenses, and small grains (Grt2) with inclusions of sillimanite in the bulk of Grt + Bt + Sil + Pl + Qz. (l) Relict grains of garnet and potassium feldspar in the bulk of Crd + Bt + Pl + Qz, mod. LP19-o5. (m) Garnet grains in gneiss, mod. RB-25; some grains are crushed and surrounded by “jackets” of biotite. In the photographs (a–d), yellow dashed lines indicate the position and direction of the microzones of plastic deformations that envelope and break the porphyroblasts of the garnet.

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8. Fig. 7. Polycrystalline inclusions in garnet from the studied metapelites. (a) An inclusion consisting of cryptocrystalline aggregates and quartz crystals in a DOV-21 garnet. (b) Crystallized inclusions with a negative crystal shape and not affected by cracks in a DOV-21 garnet. (c) Carbonate-containing inclusions in a garnet grain from a LP19-29 metapelite sample; some inclusions are affected healed cracks. (d) A detailed view of a carbonate-containing inclusion with the form of a negative crystal in a garnet grain from a sample of LP19-12 metapelite.

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9. Figure 8. Profiles of Xml and Xc values and Cr2O3, B2o3 and P2O5 contents in pomegranate grains from samples LP 19-14 and DOV-21. (a) The position of the profile in the grain of a garnet enclosed in a quartz-feldspar bulk from the LP19-14 model; biotite is present locally along the edge of the grain. (b) Profiles of XMg and XCa values and the content of Cr2O3, Sc2O3 and P2O5 in the pomegranate grain in Fig. 9a. (c) The position of the profile in the pomegranate grain, partially surrounded by a cordierite crown from the model DOV-21; dotted contours mark relict areas with an increased XCa value, one of which is crossed by the profile in Fig. 9g. (d) Profiles of XMg and XCa values and the content of Cr2O3, Sc2O3 and P2O5 in pomegranate seeds in Fig. 9b.

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10. Rhys. 9. The maps are distributed by Mg and Ca in garnet porphyroblasts from the exemplary LP19-29 (a), LP19-21 (b), LP19-08 (c), O6-19 (d), LP19-o5 (e) and RB-25 (e).

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11. Fig. 10. Distribution maps of P (a) and Cr (b) in garnet porphyroblasts from the LP19-29 model. I–III zones in porphyroblast (see the text).

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12. Fig. 11. Variations in the composition of cordierite in the studied metapelites of the Central Asian region. (a) Variations of XMg and Na content (form units) in cordierite; red diamonds indicate the average values for each sample. (b) The general dependence of the average Na content (form units) in cordierite on the Na2O content in rocks; the point for LP19-o5 deviates from the general pattern.

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13. Fig. 12. Representative Raman spectra of cordierite.

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14. Fig. 13. Fluid inclusions in quartz from metapelites. (a) Association of CO2 inclusions (HC) and water-salt inclusions (HC) in the LP 19-12 model; (b) water-salt inclusions from the LP19-o5 model.

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15. 14. Generalization of water activity data for samples LP19-14, LP19-12, LP19-29, LP19-21, O6-19 and LP19-o5 (see Supplemental 3, ESM_1–ESM_6) along the P–T trends of their metamorphic evolution (see Supplemental 2, ESM_1). The colored rectangles show aH2O variations for the average temperature and pressure indicated (in bar) next to the rectangle.

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16. Fig. 15. Generalization of the R–T trends of the studied samples. The gray rectangles and arrow marked S21 show the conditions along the P–T trend of the LP 19-11 metapelite from the Ha-Shanzi dome structure (Safonov et al., 2021). The pink area summarizes the position of the solidi of the studied rocks. I, II, III are the stages of R–T evolution (see the text).

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17. Supplementary 1
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18. Supplementary 2, ESM 1

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19. Supplementary 2, ESM 2

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20. Supplementary 2, ESM 3

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21. Supplementary 2, ESM 4

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22. Supplementary 2, ESM 5

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23. Supplementary 2, ESM 6

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24. Supplementary 2, ESM 7

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25. Supplementary 2, ESM 8

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26. Supplementary 2, ESM 9

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27. Supplementary 2, ESM 10

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28. Supplementary 3, ESM 1

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29. Supplementary 3, ESM 2

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30. Supplementary 3, ESM 3

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31. Supplementary 3, ESM 4

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32. Supplementary 3, ESM 5

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33. Supplementary 3, ESM 6

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34. Supplementary 3, ESM 7

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35. Supplementary 3, ESM 8

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36. Supplementary 3, ESM 9

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37. Supplementary 3, ESM 10

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