Introduction
The Rayner orogen, consisting of the Rayner Complex and the Eastern Ghats Belt between the Indian craton (including the Napier Complex in East Antarctica) and the Ruker craton of East Antarctica, is a large Grenville-aged (i.e. late Mesoproterozoic to early Neoproterozoic; c. 1000–900 Ma) orogen that extends for > 2000 km and has a maximum width of > 500 km (Fig. 1). This orogen was reworked by a Pan-African-aged (i.e. late Neoproterozoic to Cambrian; c. 580–500 Ma) tectonothermal event that varies in intensity from weak reworking in the northern Prince Charles Mountains (Boger et al. Reference Boger, Carson, Fanning, Hergt, Wilson and Woodhead2002, Morrissey et al. Reference Morrissey, Hand, Kelsey and Wade2016) to strong reworking in Prydz Bay (Hensen & Zhou Reference Hensen and Zhou1995, Fitzsimons et al. Reference Fitzsimons, Kinny and Harley1997). The main part of the orogen to the east is covered by ice, except for a few isolated outcrops in the vicinity of Mount Brown and the Gaussberg volcano and the Mirny Oasis along the coast of Wilhelm II Land. Some zircons from a mafic granulite and a dioritic vein from the Mirny Oasis and a lamproitic lava of the Gaussberg volcano yield ages of c. 500 Ma, suggesting that the coastal part of this area was affected by the Pan-African-aged event (Mikhalsky et al. Reference Mikhalsky, Belyatsky, Presnyakov, Skublov, Kovach and Rodionov2015). However, no new zircon growth or Pb loss associated with this event has been identified within high-grade rocks from Mount Brown (Mikhalsky et al. Reference Mikhalsky, Belyatsky, Presnyakov, Skublov, Kovach and Rodionov2015, Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). This led Mikhalsky et al. (Reference Mikhalsky, Belyatsky, Presnyakov, Skublov, Kovach and Rodionov2015) to suggest that the Pan-African-aged tectonothermal event became weaker towards inland areas. This study presents the results of combined monazite/rutile U–Pb and hornblende/biotite 40Ar/39Ar dating of metamorphic rocks collected from Mount Brown during the 2014–15 austral field season in order to determine the extent and degree of Pan-African-aged reworking in the eastern part of the Rayner orogen. The new data indicate that the Mount Brown area did indeed undergo Pan-African-aged reworking, although of relatively low grade, leading to no or partial resetting of the hornblende 40Ar/39Ar system and the complete resetting of the rutile U–Pb and biotite 40Ar/39Ar isotopic systems, without resulting in the growth of new metamorphic minerals.
Fig. 1. Geological sketch map of the Indian Ocean sector of Antarctica and adjacent parts of India and Australia prior to the breakup of Gondwana (after Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). Inset map shows the location of this region within Gondwana at c. 500 Ma.
Geological background and sampling
Mount Brown is located between Prydz Bay and the Denman Glacier in East Antarctica and is an elongate nunatak that protrudes slightly above the continental ice sheet. The outcrop area has a length of 1.5 km and a width of 50–200 m (Fig. 2) and is dominated by banded felsic orthogneisses, with subordinate amounts of layered or lenticular mafic granulites, interlayered paragneisses, anatectic leucogneisses and pegmatite veins. Zircon U–Pb dating indicates that the protoliths of the mafic granulites and felsic orthogneisses were emplaced at c. 1490–1400 Ma, with deposition of the sedimentary precursors of the paragneisses after c. 1250 Ma. These rocks subsequently underwent high-grade metamorphism and associated partial melting at c. 920–900 Ma (Mikhalsky et al. Reference Mikhalsky, Belyatsky, Presnyakov, Skublov, Kovach and Rodionov2015, Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). Petrographic textures, mineral compositions and phase equilibria modelling for a mafic granulite and a paragneiss suggest a two-stage evolution for the Grenville-aged metamorphic event, with peak pressure–temperature (P–T) conditions of 830–870°C and 7–8 kbar, followed by near-isobaric cooling to 760–830°C and 7–8.5 kbar (Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). The timing and characteristics of these geological events are similar to those recorded within the Rayner Complex in the Prince Charles Mountains–Prydz Bay region (Liu et al. Reference Liu, Zhao, Hu, Harley, Fitzsimons and Zhao2013 and references therein).
Fig. 2. Geological sketch map of Mount Brown projected on a Google Earth image (modified after Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016).
A total of seven samples from Mount Brown, including four paragneisses, two leucogneisses and one mafic granulite, were used for monazite and rutile U–Pb dating and hornblende and biotite 40Ar/39Ar dating. Paragneiss samples MB03-4, MB04-2, MB04-3 and MB04-6 contain two-stage metamorphic reaction textures defined by a coarse-grained primary (stage I) assemblage of garnet + biotite + plagioclase + quartz + ilmenite ± orthopyroxene ± rutile and a fine-grained secondary (stage II) assemblage of garnet + biotite + plagioclase + K-feldspar + quartz + ilmenite ± hornblende (Fig. 3a & b). Details of the petrographic characteristics of the paragneiss are given by Liu et al. (Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). Leucogneiss samples MB04-1 and MB04-7 have near-equigranular textures and consist of garnet, biotite, plagioclase, K-feldspar, quartz, rutile and ilmenite. Rutile is intergrown with ilmenite or occurs as individual grains (Fig. 3c). Mafic granulite sample MB04-8 has a coarse-grained primary assemblage of garnet + orthopyroxene + clinopyroxene + hornblende + biotite + plagioclase + quartz + ilmenite + magnetite (Fig. 3d), as well as a locally developed fine-grained secondary assemblage of garnet + clinopyroxene + hornblende + biotite + plagioclase + quartz + ilmenite + magnetite, as described by Liu et al. (Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). The lithologies, mineral assemblages and ages of the studied samples are summarized in Table I.
Fig. 3. Plane-polarized light photomicrographs showing mineral textures and paragenesis of paragneiss, leucogneiss and mafic granulite from Mount Brown. a. Primary mineral assemblage of garnet (g1) + biotite (bi1) + plagioclase (pl1) in paragneiss sample MB03-4. Secondary garnet corona (g2) developed around primary garnet (g1) and biotite (bi1). b. Secondary biotite (bi2), hornblende (hb), plagioclase (pl2) and K-feldspar (ksp2) developed between primary biotite (bi1) and plagioclase (pl1) in paragneiss sample MB03-4. The reaction zone also contains a visible zircon (z) crystal. c. Intergrown rutile (ru) and ilmenite (ilm) in leucogneiss sample MB04-7. d. Primary mineral assemblage of near-equigranular clinopyroxene (cpx1) + hornblende (hb1) + biotite (bi1) + plagioclase (pl1) in sample MB04-8.
Table I. Lithology, mineral assemblages and age results of the studied samples from Mount Brown.
bi = biotite, cpx = clinopyroxene, g = garnet, hb = hornblende, ilm = ilmenite, ksp = K-feldspar, mt = magnetite, opx = orthopyroxene, pl = plagioclase, q = quartz, ru = rutile.
a Zircon U–Pb ages are from Liu et al. (Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016).
Analytical techniques
Monazite U–Th–Pb analyses were performed using a sensitive high-resolution ion microprobe (SHRIMP II) at the Research School of Earth Sciences, Australian National University, Canberra, Australia. Different monazite textural domains were identified on 0.2 mm-thick thin sections that were cut and mounted on epoxy discs along with a primary Thompson Mine monazite standard (U = ~2100 ppm; radiogenic 206Pb/238U = 0.3152) and a secondary 44069 standard (424.9 Ma; Aleinikoff et al. Reference Aleinikoff, Schenck, Plank, Srogi, Fanning, Kamo and Bosbyshell2006). Internal monazite structures were revealed by back-scattered electron (BSE) imaging prior to analysis. Instrumental conditions and data acquisition followed Williams (Reference Williams1998), employing a 10 kV O2− primary ion beam with a current of ~3 nA and a diameter of ~12 µm. Common Pb corrections were made using 204Pb and the resulting data were reduced using the in-house PRAWN and LEAD software (T.R. Ireland). Finally, ages were calculated using the constants recommended by the International Union of Geological Sciences (IUGS) Subcommission on Geochronology and were determined using ISOPLOT. Uncertainties for individual analyses are reported as one standard deviation (1σ) and calculated weighted mean 206Pb/238U or 207Pb/206Pb ages are quoted at the 95% confidence level. The results of these analyses are given in Table SI.
Rutile U–Pb analyses were undertaken by secondary ionization mass spectrometry (SIMS) with a Cameca IMS-1280 large radius instrument at the Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing, China. Rutile was extracted from samples using conventional crushing, sieving, heavy liquid separation and handpicking techniques. The resulting rutile was mounted in epoxy discs together with rutile standards R10 (U = ~30 ppm; concordia age = 1090 ± 5 Ma; Luvizotto et al. Reference Luvizotto, Zack, Meyer, Ludwig, Triebold and Kronz2009), 99JHQ-1 (highly variable U content with an average of 2 ppm; 206Pb/238U age = 218 ± 1.2 Ma; Li et al. Reference Li, Li, Zheng, Li, Massonne and Wang2003) and in-house megacrystic JDX (U = ~6 ppm; 207Pb/206Pb age = 521 Ma; 206Pb/238U age = 520–500 Ma; Li et al. Reference Li, Lin, Su, Li, Shi, Liu and Tang2011). The mount was then polished to expose the fresh interior of the rutile crystal. Internal rutile structures were determined by BSE imaging before SIMS analysis using the instrument setup and analytical procedures outlined by Li et al. (Reference Li, Li, Zheng, Li, Massonne and Wang2003, Reference Li, Lin, Su, Li, Shi, Liu and Tang2011). This analysis used a primary O2− ion beam accelerated at 13 kV, with an intensity of ~15 nA. An aperture illumination node (Kohler illumination) was used with a ~200 µm aperture to produce even sputtering over the entire area of analysis. The ellipsoidal spot was ~20 × 30 µm in size and positive secondary ions were extracted using a 10 kV potential. The analysis used a mass resolution of ~6000 and the magnet was cyclically peak-stepped through a sequence including 206Pb+, 207Pb+, 208Pb+, U+, UO+, ThO+, UO2+ and 49TiO4+ to produce a single dataset for each analysis. A single ion-counting electron multiplier was used as the detection device and the 49TiO4+ signal was used as a reference peak for centring of the secondary ion beams because this peak is sufficiently intense and is free of interference from ZrO. Each measurement consisted of 10 cycles and the total analytical time per single analysis was ~15 min. Common Pb corrections used the 207Pb-based method (Williams Reference Williams1998, Li et al. Reference Li, Lin, Su, Li, Shi, Liu and Tang2011). Ages were again calculated using ISOPLOT and age regressions are quoted at the 95% confidence level. The results of these analyses are given in Table SII.
Hornblende and biotite 40Ar/39Ar analyses were conducted using a MAP-215/50 mass spectrometer at the College of Earth, Ocean and Atmospheric Sciences, Oregon State University, Corvallis, OR, USA. Hornblende and biotite were extracted using crushing, sieving, heavy liquid separation and handpicking techniques. The samples were then prepared for analysis using the approach outlined by Duncan & Keller (Reference Duncan and Keller2004). Separated minerals were placed in evacuated quartz tubes that were wrapped in Cu foil with unknowns alternating with packages of the FCT-NM sanidine monitor standard (28.201 ± 0.023 Ma; Kuiper et al. Reference Kuiper, Deino, Hilgen, Krijgsman, Renne and Wijbranset2008). The resulting Cu foil-wrapped samples were irradiated for 6 h in the TRIGA nuclear reactor ICIT facility at Oregon State University. Irradiation parameter J values were estimated using parabolic interpolation, yielding uncertainties of 0.2–0.3% (Koppers et al. Reference Koppers, Staudigel and Wijbrans2000). Interfering K and Ca reactions were corrected using the approaches outlined by Koppers et al. (Reference Koppers, Staudigel and Wijbrans2000). The 40Ar/39Ar data were obtained using incremental heating, with incremental heating plateau and isochron ages calculated using the ArArCALC v2.4 software package (Koppers Reference Koppers2002). 40Ar/39Ar ages are reported with 1σ uncertainties, and 46–53 heating steps for each sample were performed to yield plateau ages that are defined by 9–43 heating steps. The complete experimental data and associated diagrams are given in Table SIII.
Results
Monazite U–Pb dating
Monazite from paragneiss samples MB04-2, MB04-3 and MB04-6 is present as inclusions in primary minerals such as garnet, biotite, plagioclase and quartz (type I; Fig. 4a & b), as intergranular crystals in the matrix (type II; Fig. 4c), as individual grains in fine-grained biotite + plagioclase + K-feldspar + quartz + ilmenite ± garnet symplectites (type III; Fig. 4d–f) and as globular beads either in symplectites or around garnet porphyroblasts (type IV; Fig. 4g & h). The majority of monazite is ovoid, prismatic or irregular and has grain sizes of 20–400 µm, although the beaded monazite is commonly isometric with grain sizes of 20–40 µm. Monazite grains are typically zoned in BSE images and have a relatively dark core and a bright rim (Fig. 4a, e & f). Some grains show reverse zoning patterns (Fig. 4b) and some are homogenous (Fig. 4c). Rare grains in sample MB04-3 have a cloudy-zoned core (Fig. 4d).
Fig. 4. Representative back-scattered electron images of monazite from paragneisses from Mount Brown. a. Monazite from sample MB04-3 occurring as an inclusion in garnet and showing a dark core and a bright, discontinuous rim. b. Monazite from sample MB04-3 occurring as an inclusion in biotite and showing a bright core and a dark rim. c. Monazite from sample MB04-2 located between garnet and biotite and having a homogeneous structure. d. Monazite from sample MB04-3 hosted by a symplectite and showing a cloudy-zoned core and a bright rim. e. & f. Monazite from sample MB04-3 hosted by a symplectite and showing a dark core and a bright rim. g. & h. Monazite from samples MB04-3 and MB04-6 occurring as globular beads around garnet porphyroblast and showing a dark core and a bright rim. Circles with numbers indicate SHRIMP analytical spots with their identification numbers. Ages are given with 1σ uncertainties. bi = biotite, g = garnet, ilm = ilmenite, ksp = K-feldspar, mnz = monazite, pl = plagioclase, q = quartz.
A total of 87 SHRIMP spot analyses of 65 monazite grains from three samples yield variable Th and U concentrations that are indistinguishable between cores and rims (U = 0.08–0.93 wt.%, Th = 0.03–27.26 wt.% and Th/U = 0.19–95.69). Twenty-five spot analyses from sample MB04-2 yield 206Pb/238U ages ranging from 929 ± 17 to 633 ± 12 Ma; of these, 12 older spots (excluding spot 1.1c with a large uncertainty) on 9 cores and 2 rims of types I and II monazite and 1 core of type III monazite give a weighted mean age of 908 ± 9 Ma (mean square weighted deviation [MSWD] = 0.69) (Fig. 5a & b). The youngest age of 633 ± 12 Ma is produced by a type IV monazite grain. Seven spot analyses of cloudy-zoned monazite cores from sample MB04-3 yield old 207Pb/206Pb ages varying from 1344 ± 10 to 1052 ± 14 Ma. The remaining 41 spots yield 206Pb/238U ages between 930 ± 14 and 621 ± 10 Ma. Among them, 14 older spots on 6 cores and 1 rim of types I and II monazite and 5 cores and 2 rims of type III monazite give a weighted mean age of 909 ± 8 Ma (MSWD = 0.89), whereas 4 younger spots on type IV monazite grains produce a weighted mean age of 633 ± 11 Ma (MSWD = 0.98) (Fig. 5c & d). Fourteen spot analyses from sample MB04-6 yield 206Pb/238U ages ranging from 958 ± 17 to 661 ± 13 Ma; of these, 7 older spots on 5 cores and 1 rim of types I and II monazite and 1 rim of type III monazite give a weighted mean age of 910 ± 31 Ma (MSWD = 4.3) (Fig. 5e & f). One type IV monazite grain yields a younger age of 676 ± 22 Ma; another analytical spot, which deviated slightly from such a grain, produces an age of 676 ± 22 Ma (2.1c; not shown in Fig. 5e).
Fig. 5. SHRIMP U–Pb concordia diagrams and distribution plots of 206Pb/238U ages for monazite from paragneisses from Mount Brown. a. & b. Monazite from sample MB04-2. c. & d. Monazite from sample MB04-3. e. & f. Monazite from sample MB04-6.
Statistically, 206Pb/238U apparent age trends are shown in Fig. 6 and are summarized as follows: 1) types I and II monazite tend to yield older ages relative to type III monazite, which yields relatively young ages, 2) monazite cores are older than monazite rims barring a grain from sample MB04-6, and 3) all type IV monazite grains, except for a deviated analytical spot from sample MB04-6 (2.1c; not shown in Fig. 6), yield almost the youngest age cluster in each sample.
Fig. 6. Cumulative probability histogram showing the distribution of monazite U–Pb ages for paragneisses from Mount Brown.
Rutile U–Pb dating
The dated rutile from sample MB04-1 has grain sizes of 50–150 µm. A total of 25 SIMS spot analyses of 25 rutile crystals yielded U concentrations of 0.8–27.0 ppm and common 206Pb values from 1% to 72%. Plotting the results of these analyses on a Tera–Wasserburg plot yields a linear regression (excluding four data points with large uncertainties) that defines a lower intercept age of 515 ± 12 Ma (n = 21, MSWD = 2.0) (Fig. 7a), which is consistent with the weighted mean 206Pb/238U age of 516 ± 15 Ma (n = 7, MSWD = 1.4) obtained for the near-concordant data from this sample (Fig. 7b).
Fig. 7. Secondary ionization mass spectrometry U–Pb concordia diagrams and distribution plots of 206Pb/238U ages for rutile from leucogneisses from Mount Brown. a. & b. Rutile from sample MB04-1. c. & d. Rutile from sample MB04-7.
The dated rutile from sample MB04-7 is 200–400 µm in diameter. A total of 30 spot analyses of 30 rutile crystals yielded U concentrations of 5.7–160.9 ppm and common 206Pb values are generally < 10%, although some values lie between 12% and 76%. A regression of these data points (excluding two outliers) on a Tera–Wasserburg plot yields a lower intercept age of 520 ± 8 Ma (n = 28, MSWD = 1.16) (Fig. 7c), which is within uncertainty of the weighted mean 206Pb/238U age of 515 ± 10 Ma (n = 17, MSWD = 0.82) obtained for the near-concordant data from this sample (Fig. 7d).
Hornblende and biotite 40Ar/39Ar dating
Hornblende and biotite subjected to dating are all coarse-grained crystals that formed during stage I metamorphism. Stage II minerals from mafic granulite (sample MB04-8) and paragneiss (samples MB03-4 and MB04-3) are too fine to be separated. Hornblende from mafic granulite sample MB04-8 yields a plateau age of 743.93 ± 5.46 Ma (MSWD = 71.36) defined by 85.59% of the total 39Ar released (Fig. 8a). In contrast, biotite from mafic granulite (sample MB04-8), paragneiss (samples MB03-4 and MB04-3) and leucogneiss (samples MB04-1 and MB04-7) yields plateau ages ranging from 521.21 ± 1.19 Ma (MSWD = 1.38) to 505.08 ± 1.01 Ma (MSWD = 1.30) defined by 40.52–99.61% of the total 39Ar released (Fig. 8b–f).
Fig. 8. 40Ar/39Ar plateau age spectra for hornblende and biotite from different rock types from Mount Brown. a. Hornblende from mafic granulite sample MB04-8. b. Biotite from mafic granulite sample MB04-8. c. Biotite from paragneiss sample MB03-4. d. Biotite from paragneiss sample MB04-3. e. Biotite from leucogneiss sample MB04-1. f. Biotite from leucogneiss sample MB04-7.
Discussion
Interpretation of monazite/rutile U–Pb and hornblende/biotite 40Ar/39Ar ages
As the Pb closure temperature of monazite is thought to be > 900°C (Cherniak et al. Reference Cherniak, Watson, Grove and Harrison2004), this accessory mineral is frequently used to date medium- to high-grade metamorphism. In situ U–Pb dating of monazite from three paragneisses from Mount Brown yielded three groups of age data, each of which is geologically significant. Apart from one young age that may have been affected by later Pb loss, the oldest age group of c. 1340–1180 Ma obtained from cloudy-zoned monazite cores from sample MB04-3 is similar to the detrital zircon ages of c. 1500–1250 Ma obtained for the same sample (Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). However, it is unclear whether these inherited monazite ages reflect the timing of earlier magmatic, diagenetic or metamorphic events. The major age group of c. 910 Ma determined by the analysis of granular monazite of types I–III is consistent with the ages of c. 920–900 Ma obtained for zircon overgrowth domains in diverse metamorphic rock types in this area (Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016), reflecting the timing of the Grenville-aged high-grade metamorphism. The young age group of c. 670–630 Ma was generally obtained from small globular beads of type IV monazite (< 40 µm) around garnet porphyroblasts or hosted by symplectites. These monazites are thought to have formed as a result of dissolution–reprecipitation processes associated with a low-temperature fluid flow event that did not affect the major mineral assemblages in the rocks (e.g. Harlov et al. Reference Harlov, Wirth and Hetherington2011, Williams et al. Reference Williams, Jercinovic, Harlov, Budzyn and Hetherington2011, Kelly et al. Reference Kelly, Harley and Möller2012). Although type III monazite tends to yield younger ages than types I and II monazite, the fact that some of these monazite grains yield ages > 900 Ma and that their grain sizes are clearly larger than those of syplectitic minerals suggest that these younger ages resulted from the recrystallization of monazite rather than any new growth of it. The cores or rims of some type I monazite grains included in garnet, biotite, plagioclase and quartz also yield relatively young ages (c. 870–760 Ma; see spots 17.1c and 21.1c from sample MB04-2 and spots 11.1c, 25.2r and 27.1c from sample MB04-3 in Table SI), further indicating Pb loss in monazite probably due to slow cooling or the reworking of the Pan-African-aged tectonothermal event. This suggests that any monazite ages between c. 900 and c. 670 Ma reflect the timing of isotopic resetting and may have no geological meaning.
The rutile U–Pb dating of the two leucogneisses yielded ages of c. 520–515 Ma, similar to the biotite 40Ar/39Ar ages of c. 520–505 Ma obtained from mafic granulite, paragneiss and leucogneiss. However, dating of hornblende from a mafic granulite yielded a 40Ar/39Ar plateau age of 743.93 ± 5.46 Ma, which is older than the U–Pb ages of rutile and the 40Ar/39Ar plateau ages of biotite. In general, in high-temperature terranes, rutile U–Pb and hornblende/biotite 40Ar/39Ar ages reflect the timing of cooling of these minerals through the closure temperature (T c) of their isotopic systems. The T c of the 40Ar/39Ar system is 535 ± 50°C for hornblende and 320 ± 30°C for biotite (McDougall & Harrison Reference McDougall and Harrison1999). However, the T c of the rutile U–Pb system remains controversial and appears to be significantly grain size dependent. Although experimental studies on the diffusion of Pb within rutile suggested a high T c of ≥ 600°C for a grain size of 100 µm (Cherniak Reference Cherniak2000), numerous field-based studies have demonstrated a relatively low T c of 450 ± 50°C (Mezger et al. Reference Mezger, Hanson and Bohlen1989, Li et al. Reference Li, Li, Zheng, Li, Massonne and Wang2003, Reference Li, Lin, Su, Li, Shi, Liu and Tang2011, Zack et al. Reference Zack, Stockli, Luvizotto, Barth, Belousova, Wolfe and Hinton2011). Our study supports the latter and offers further evidence that the T c of the rutile U–Pb system is lower than that of the hornblende 40Ar/39Ar system. Given that all of the minerals dated during this study formed during Grenville-aged high-grade metamorphism, there are three possibilities for interpreting the age difference between hornblende, rutile and biotite in the study area. The first is that the Grenville-aged high-grade rocks slowly cooled through ~535°C by 744 Ma and then to below ~450°C during the period 520–505 Ma, with a cooling rate of ~0.5–2.0°C/myr over c. 400 myr (path I in Fig. 9). Post-tectonic slow cooling with similar rates of 1–3°C/myr has been documented to occur in many deeply eroded high-grade Precambrian orogens (e.g. Willigers et al. Reference Willigers, Van Gool, Wijbrans, Krogstad and Mezger2002). The second is that the rocks underwent a Pan-African-aged reheating event after slow cooling, with a reheating temperature greater than the hornblende Ar closure temperature (path II in Fig. 9). The third is that the Pan-African-aged tectonothermal event reheated the rocks that have rapidly cooled after Grenville-aged high-grade metamorphism (path III in Fig. 9), leading to the partial resetting of the hornblende 40Ar/39Ar system and the complete resetting of the rutile U–Pb and biotite 40Ar/39Ar systems. We infer that the second or third interpretations are more probable, as the Pan-African-aged tectonothermal event represents an independent orogenic cycle in the Prince Charles Mountains–Prydz Bay region (Liu et al. Reference Liu, Zhao, Hu, Harley, Fitzsimons and Zhao2013) and is also likely to have affected the Mount Brown area. The extremely rapid cooling from ~450°C to 320°C after 520 Ma, as indicated by the high similarity of rutile U–Pb and biotite 40Ar/39Ar ages, is discordant with the assumed earlier slow cooling, lending support to these interpretations.
Fig. 9. Possible temperature–time cooling/reheating paths for high-grade rocks from Mount Brown.
The high-grade metamorphic rocks from Mount Brown record two major stages of mineral growth. Both of the resulting mineral assemblages formed during a single Grenville-aged metamorphic cycle, as evidenced by the fact that some zircon grains located in areas of retrograde reaction textures in paragneisses also yield early Neoproterozoic ages (Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). The following three lines of evidence support this assumption: 1) the compositions of stage I garnet increase in grossular contents towards garnet rims that have compositions similar to stage II garnet (Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016), indicating that they record a continuous metamorphic process, 2) petrographic observations indicate that the globular beads of monazite with c. 670–630 Ma ages grew after the formation of the coronal and symplectitic minerals, and 3) the new growth of monazite at c. 580–500 Ma did not occur in areas with symplectitic textures that formed at higher P–T conditions of 760–830°C and 7.0–8.5 kbar (Liu et al. Reference Liu, Wang, Zhao, Liu, Chen, Cui and Song2016). This demonstrates that no metamorphic reactions occurred in these rocks after the Grenville-aged metamorphic event. In fact, the temperature of the Pan-African-aged tectonothermal event at Mount Brown remains unclear. Although monazite has a high Pb closure temperature, it can form under greenschist facies conditions (≤ 450°C; Franz et al. Reference Franz, Andrehs and Rhede1996, Townsend et al. Reference Townsend, Miller, D'Andrea, Ayers, Harrison and Coath2000). The small beaded monazite in the samples from the area is also suggestive of relatively low-temperature hydrothermal activity, as has been documented for similar monazite grains in high-grade metamorphic terranes (e.g. Chen et al. Reference Chen, Liu, Lee, Xiang and Zhou2012). Considering that the c. 650–600 Ma tectonothermal event has not been recognized in the Rayner Complex, we infer that the hydrothermal fluid flow event that formed the beaded monazite is likely to reflect localized processes. On the other hand, the c. 580–500 Ma tectonothermal event failed to completely reset the hornblende 40Ar/39Ar system, providing evidence of temperature conditions that were not significantly higher than the hornblende Ar closure temperature (i.e. ~535°C).
Implications for the impact of the Pan-African-aged tectonothermal event
The available data suggest that the Pan-African-aged tectonothermal event affected the vast outcrops in the Prince Charles Mountains–Prydz Bay region (Liu et al. Reference Liu, Zhao, Hu, Harley, Fitzsimons and Zhao2013). The recent reports of zircon age records of c. 590–500 Ma in limited outcrops in the Enderby, Wilhelm II and Queen Mary lands indicate that the western and eastern parts of the Rayner Complex were also reworked during the Pan-African-aged event (Mikhalsky et al. Reference Mikhalsky, Belyatsky, Presnyakov, Skublov, Kovach and Rodionov2015, Horie et al. Reference Horie, Hokada, Motoyoshi, Shiraishi, Hiroi and Takehara2016, Daczko et al. Reference Daczko, Halpin, Fitzsimong and Whittaker2018, this paper). However, the metamorphic grade of Pan-African-aged reworking varies between different areas or terranes, from granulite facies in the Rayner Complex in Prydz Bay (760–860°C and 6–7 kbar; Fitzsimons Reference Fitzsimons1996, Carson et al. Reference Carson, Powell, Wilson and Dirks1997) and the northern Prince Charles Mountains (800–870°C and 5.5–6.5 kbar; Morrissey et al. Reference Morrissey, Hand, Kelsey and Wade2016), to upper amphibolite facies in the Lambert Terrane (650–700°C and 6–7 kbar; Boger & Wilson Reference Boger and Wilson2005), lower amphibolite facies in the Ruker Terrane (565–640°C and 4–5.2 kbar; Phillips et al. Reference Phillips, White and Wilson2007) and the Fisher Terrane (550–615°C and 2.5–4.0 kbar; Van Leeuwen et al. Reference Van Leeuwen, Morrissey, Kelsey and Raimondo2019) and greenschist facies in a subglacial Archean block south-east of the Vestfold Hills (chloritoid grade; our unpublished data). Rarer ultrahigh-temperature and high-pressure granulite facies metamorphism has also been identified in the Rauer Group (950–1050°C and 9.5–12.0 kbar; Harley Reference Harley1998, Kelsey et al. Reference Kelsey, White, Powell, Wilson and Quinn2003, Tong & Wilson Reference Tong and Wilson2006) and in the Grove Mountains (770–840°C and 11.6–14.0 kbar; Liu et al. Reference Liu, Hu, Zhao, Lou, Wei and Liu2009, Chen et al. Reference Chen, Wang, Liu and Zhao2018), respectively. Therefore, any tectonic model for the Pan-African-aged orogeny in the Indian Ocean sector of Antarctica should incorporate the extent and variability of the metamorphic reworking.
The degree and behaviour of Pan-African-aged reworking also vary spatially within individual areas or terranes. In the case of the Rayner Complex, the most intense metamorphic reworking occurs in the Prydz Bay area and causes penetrative deformation, regional granulite facies metamorphism and widespread partial melting. This leads to the formation of new zircon and monazite in high-grade rocks during the Pan-African-aged period (e.g. Fitzsimons et al. Reference Fitzsimons, Kinny and Harley1997, Kelsey et al. Reference Kelsey, Hand, Clark and Wilson2007). In contrast, high-temperature reworking in the northern Prince Charles Mountains only occurs in discrete locations and is characterized by the development of Pan-African-aged monazite-bearing mineral reaction zones without any new zircon growth (Morrissey et al. Reference Morrissey, Hand, Kelsey and Wade2016). Mount Brown provides evidence of another type of thermal reworking that causes the isotopic resetting of some minerals and is not associated with the growth of any new phases. This is similar to the expression of polymetamorphism in the south-western Vestfold Hills, where mineral–whole-rock Sm–Nd ‘isochron’ ages for metamorphic rocks range from 670 ± 7 to 589 ± 22 Ma, whereas hornblende and biotite 40Ar/39Ar ages cluster between 526 ± 4 and 509 ± 3 Ma (Liu et al. Reference Liu, Zhao, Hu, Harley, Fitzsimons and Zhao2013), and there are no mineral reaction textures associated with the Pan-African ages. In fact, in the absence of penetrative deformation and intensive fluid infiltration, relatively dry granulite facies rocks are rather inert during high-temperature reworking (Morrissey et al. Reference Morrissey, Hand, Kelsey and Wade2016). This means that earlier mineral assemblages are commonly preserved during later metamorphic overprinting, as is the case in numerous polymetamorphic terranes (Morrissey et al. Reference Morrissey, Hand, Kelsey and Wade2016 and references therein). Despite this, some geochronometers with relatively low closure temperatures can still record the timing of such reworking events.
Conclusions
Almost all of the tectonic units of the Grenville-aged Rayner orogen between the Indian craton (including the Napier Complex in East Antarctica) and the Ruker craton of East Antarctica were affected by the Pan-African-aged tectonothermal event, although varying in metamorphic grade, reworking intensity and mineral growth behaviour. At the eastern part of the Rayner Complex, high-grade metamorphic rocks from Mount Brown only underwent a relatively low-temperature reworking during the Pan-African-aged event, leading to the growth of small monazite beads at c. 670–630 Ma, no or partial resetting of the hornblende 40Ar/39Ar system and the complete resetting of the rutile U–Pb and biotite 40Ar/39Ar isotopic systems at c. 520–505 Ma. This suggests that, in the absence of penetrative deformation and intensive fluid infiltration, the complete isotopic resetting of some minerals may occur without the formation of new mineral assemblages in polymetamorphic terranes.
Acknowledgements
Daniel P. Miggins of Oregon State University kindly performed hornblende and biotite 40Ar/39Ar analyses. James Hamilton and Yingchun Cui are thanked for their assistance during fieldwork as part of the 2014–15 Chinese National Antarctic Research Expedition. Logistic support from the Australian Antarctic Division and Chinese Arctic and Antarctic Administration is also gratefully acknowledged. Critical reviews by Evgenii Mikhalsky and Laura Morrissey substantially improved the manuscript.
Author contributions
XL conceived the study and wrote the paper. BF and QL performed the monazite and rutile U–Pb analyses, respectively. JL and HC assisted in field sampling. YZ commented on the manuscript.
Financial support
This research was supported by the National Natural Science Foundation of China (No. 41530209), Central Public-Interest Scientific Institution Basal Research Fund (No. JYYWF201819) and Geological Investigation Project of the Chinese Geological Survey (No. DD20190579).
Supplemental material
Supplemental tables and figures will be found at https://doi.org/10.1017/S0954102019000518.
Open access
