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2.1–1.85Ga tectonic events in the Yangtze Block, South China:Petrological and geochronological evidence from the Kongling Complexand implications for the reconstruction of supercontinent Columbia
Changqing Yin a,b, Shoufa Lin a,c,⁎, Donald W. Davis d, Guochun Zhao e, Wenjiao Xiao b,Longming Li a,b, Yanhong He f
a Department of Earth and Environmental Sciences, University of Waterloo, 200 University Avenue West, Waterloo, Ontario N2L 3G1, Canadab State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, Chinac School of Resources and Environment, Hefei University of Technology, Hefei 230026, Chinad Department of Earth Sciences, University of Toronto, 22 Russell Street, Toronto, Ontario M5S 3B1, Canadae Department of Earth Sciences, University of Hong Kong, Pokfulam Road, Hong Kong, Chinaf Department of Geology, Northwest University, Xi'an 710069, China
This paper presents petrography, zircon U–Pb ages and Hf isotopic data as well as whole-rock Sm–Nd isotopicdata for mafic granulites, metapelitic rocks and high-grade marble from the Kongling Complex in the YangtzeBlock, South China. Petrographic observations indicate that these three types of rocks experienced high-pressure metamorphism. Their mineral assemblages and P–T conditions define a clockwise P–T path involvingisothermal decompression following the peak high-pressure metamorphism, which is considered to record acontinent–continent collisional event. This is systematic documentation of the tectonic evolution of the KonglingComplex from 2.1-2.0Ga deposition (constrained by youngest detrital zircon and metamorphic zircon) through~2.0 Ga collision (high-pressure metamorphism) and syn-collisional partial melting (S-type granite andmigmatization of TTG gneiss) to ~1.85 Ga post-collisional extension (A-type high-K granite and mafic dyke).These ages are broadly coincident with global collisional events (2.1–1.8 Ga) that led to the assembly of thePalaeo-Mesoproterozoic Columbia (or Nuna) supercontinent. Therefore, this study provides strong evidencethat the Yangtze Block in South China was a component of the Columbia supercontinent.
The Yangtze Block in South China is a major cratonic block that isbelieved to have been involved in the assembly of many ancientsupercontinents such as Columbia, Rodinia and Pangea (Cawood et al.,2013; Evans, 2009; Li et al., 2008; Veevers, 2004; Yu et al., 2008, 2012;Zhao et al., 2002, 2004; Zhang et al., 2012a,b,c). Therefore, its formationand evolution can provide significant insights into crustal accretion andamalgamation of the supercontinents. However, our attention hasmainly been focused on the younger supercontinents Pangea andRodinia (Bader et al., 2013; Condie, 2002; Dalziel et al., 2000; Meertand Powell, 2001; Torsvik, 2003). In contrast, understanding of theearlier, Palaeo-Mesoproterozoic Columbia supercontinent has beenmore tenuous. Columbia contained almost all of the world's continentalblocks that were amalgamated along global 2.1–1.8 Ga collisionalorogens (Zhao et al., 2002). However, it remains controversial whetherthe South China was part of the Columbia supercontinent and, if so,
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where it was located within this supercontinent (Evans, 2009; Zhanget al., 2012a; Zhao et al., 2002). A main reason for this controversy isthat no typical 2.1–1.8 Ga continent–continent collision has beenidentified in South China.
The Kongling Complex, located in the north of the Yangtze Block inSouth China and composed of Mesoarchean TTG basement rocks andthe Palaeoproterozoic Kongling Group (metamorphic sedimentaryrocks), is considered to have been involved in global collisional events(2.1–1.8 Ga) that led to the assembly of the Columbia supercontinent(Wu et al., 2009; Zhang et al., 2006b,c; Zhao et al., 2002). However,tectonic setting and evolution of the Kongling Complex remain unknownor controversial, due to the absence of high-pressure granulite and thelack of precise constraints on timing of deposition and metamorphismin the Kongling Group. In this paper, we report high-pressure maficgranulite in the Kongling Complex and determine depositional andmetamorphic timing of the Kongling Group based on petrography,zircon U–Pb ages and Hf isotopic data, and whole-rock Nd isotopicdata on high-pressure mafic granulites, metasedimentary rocksand high-grade marble from the Kongling Complex. The results ofthis study provide strong evidence that the South China is a
component of the Palaeo- to Mesoproterozoic Columbia super-continent and provide significant insights into understanding thereconstruction of the supercontinent.
2. Geologic setting
The South China Craton is separated from the North China Craton bythe Qinling–Dabie–Sulu orogen in the north, from the Songpan–GanzeTerrane by the Longmenshan Fault in the west, and is bounded by thePacific Ocean to the southeast (Fig. 1; Zhao and Cawood, 2012). It isconventionally subdivided into the Yangtze Block to the northwest andthe Cathaysia Block to the southeast (Fig. 1). The Archean and Palaeo-proterozoic basement of the South China Craton has only been exposedin the northern and western parts of the Yangtze Block, represented bythe Kongling Complex, Huangtuling granulites, Yudongzi Group andHouhe Complex in the north, and by the Dahongshan and Dongchuangroups in the southwest (Fig. 1; Chen et al., 2013a,b; Wang et al., 2013;Wu et al., 2008, 2012; Zhao and Cawood, 2012; Zheng et al., 2004,2006), and in the northeastern part of Cathaysia (Xia et al., 2012; Yuet al., 2008, 2012). The dominant Precambrian rocks in the South ChinaCraton are Neoproterozoic rocks (Dong et al., 2012; Wang et al., 2012a,b,c,d; Zhang et al., 2012b,c, 2013).
The Kongling Complex, covering an area of ~360km2 (Fig. 1; Gao et al.,1999), consists predominantly of Archean tonalitic–trondhjemitic–granitic (TTG) gneisses and Palaeoproterozoic Al-rich metasedimentaryrocks (supracrustal rocks), with minor amphibolite, mafic granulitesand S-type garnet-bearing granites (Fig. 2; Gao et al., 1999, 2011).Traditionally, these Al-rich supracrustal rocks and the associatedamphibolite and mafic granulites are together called the ‘KonglingGroup’. It is intruded by ~1.85Ga Quanyishang K-feldspar granite in thenorth and the early Neoproterozoic (850–826Ma) Huangling granitoidsin the south, and surrounded by the unmetamorphosed late Neo-proterozoic and Palaeozoic sedimentary cover (Fig. 2; Peng et al., 2012;Xiong et al., 2008; Zhang et al., 2008, 2009; Zhang and Zheng, 2013;Zhao and Guo, 2012; Zhao et al., 2013a,b,c).
Fig. 1. Schematic tectonic map of China showing major PreAfter Zhao and Cawood (2012).
The Kongling Group can be subdivided into three “formations”: thebottom formation is composed predominantly of graphite–sillimanite–garnet gneiss and staurolite–sillimanite–garnet gneiss, with minorgarnet–biotite schist and amphibolite; the middle formation consistsmainly of graphite–biotite schist, olivine–diopside marble, calc–silicaterock and quartzite; and the top formation is dominated by bandedfine-grained biotite–plagioclase gneiss, locally including BIFs, calc–silicate, mafic granulite and amphibolite lenses and/or boudins.
Available geochronological data show that major TTG gneisses fromthe Kongling Complex were emplaced in the period of 3.3–3.2 Ga and3.0–2.9 Ga and metamorphosed at 2015–1891 Ma (Gao et al., 1999,2001, 2011; Jiao et al., 2009; Peng et al., 2009, 2012; Qiu et al., 2000;Wu et al., 2009; Zhang et al., 2006a,b; Zheng and Zhang, 2007). Thepreviously-documented youngest detrital zircon from the meta-sedimentary rocks in the Kongling Complex constrained the maximumdepositional age at ∼2.87 Ga (Qiu et al., 2000). The Hf isotopic datareveal that the 3.3–3.2Ga and 3.0–2.9Ga zircons from the TTG gneissesand metasedimentary rocks in the Kongling Complex are characterizedby negative εHf(t) values and 3.5–4.0 Ga Hf model ages (Gao et al.,2011; Jiao et al., 2009; Liu et al., 2008; Zhang et al., 2006a; Zheng andZhang, 2007).
3. Petrography
The protoliths of mafic, pelitic and carbonate-bearing rock-typesfrom the Kongling Complex underwent high-grade metamorphism. Inthis paper, representative samples of high-pressure mafic granulite(11YC01-6, Fig. 3a), garnet–sillimanite gneisses (11YC02-2, Fig. 3b) andolivine–diopside marble (11YC05-7, Fig. 3c) were selected for petro-graphic analyses.
Fig. 2. Geologic map of the Kongling Complex: stars showing the sampling locations. Abbreviations: Grt= garnet; Sill= sillimanite.
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(q). These minerals have commonly a relatively large grain size andanhedral character and are interpreted as being part of a primaryassemblage. They are surrounded by coronae containing fine-grainedorthopyroxene (opx), hornblende (hb), plagioclase and ilmenite(Fig. 4a). Symplectitic intergrowths of orthopyroxene and plagioclase,locally with amphibole, replace garnet where it is in contact withclinopyroxene (Fig. 4a). Orthopyroxene + plagioclase symplectitesbetween garnet and clinopyroxene suggest a reactional equilibrium as
Fig. 3. Field photographs showing outcrops of (a) high-pressuremafic granulite (sample 11YC0111YC05-7) and (d) S-type garnet-bearing granite (11YC06-1). Abbreviations: Grt= garnet; Ol
follows (Guo et al., 2002; Harley, 1989; Kumar and Chacko, 1994; Tamet al., 2012; Thost et al., 1991; Zhao et al., 2001):
Fig. 4. Photomicrographs showing the mineral assemblages and textures of the high-grade rocks and S-type garnet-bearing granite from the Kongling Complex. (a) High-pressure maficgranulite: symplectitic intergrowths of orthopyroxene+plagioclase between hornblende and garnet+clinopyroxene (sample 11YC01-6). (b) Sillimanite–garnet gneiss: sillimanite andK-feldspar around garnet, showing a weak preferred orientation parallel to the regional foliation; sillimanite occurs both as fibrous aggregates and as larger crystals. (c) Olivine–diopsidemarble: olivine, diopside and calcite in the matrix (sample 11YC05-7). (d) S-type garnet-bearing granite: garnet, K-feldspar, plagioclase, biotite and quartz in the matrix (11YC06-1).Abbreviations: grt=garnet; opx=orthopyroxene; cpx=clinopyroxene; hb=hornblend; pl=plagioclase; sill=sillimanite; bi=biotite; ksp=K-feldspar; st=staurolite; ol=olivine;di= diopside; cc= calcite.
16
17g cpx hb ru ilm
g cpx pl ru ilm flg cpx plru
NCFMASHTO (+q)
203C. Yin et al. / Lithos 182–183 (2013) 200–210
assemblage (M2) develops reactional coronitic textures around M1
minerals. It comprises opx+pl+hb+cpx+ilmand reflects equilibrationin the low-pressure granulite facies. The Phase relations weremodeled inthe chemical systemNa2O–CaO–FeO–MgO–Al2O3–SiO2–H2O–TiO2–Fe2O3
(NCFMASHTO) on the basis of the bulk-rock composition of sample11YC01-6. In Fig. 5, the P–T conditions of M1 and M2 assemblages areN12 kbar, 870 °C; and b9 kbar, b850 °C, respectively. They define aclockwise P–T path involving isothermal decompression (ITD), whichsuggests a continent–continent collision tectonic setting (England andThompson, 1984; Thompson and England, 1984).
650 700 750 800 850 900 9507
8
9
10
11
12
13
14
15g cpx pl hb ru ilm
g cpx pl hb ilm
g cpx opx pl hb ilm
cpx opx pl hb ilm
cpx opx pl ilm fl
hb ilm fl
g cpx pl hb ilm fl
g cpx pl ilm fl
1 2
3
g opx cpx pl hb ilm flg opx cpx pl ilm flopx cpx pl hb ilm fl
M1
M2
Fig. 5. A P–T pseudosection calculated for a high-pressure mafic granulite sample(11YC01-6) with bulk compositions: H2O = 0.980, SiO2 = 53.673, Al2O3 = 8.099,CaO = 11.475, MgO = 8,822, FeO = 11.436, Na2O = 2.465, TiO2 = 0.881, O = 2.168 inmol.%, with H2O sufficient to just saturate the solidus for a given mineral assemblage ataround 6 kbar. A clockwise P–T path involving isothermal decompression (ITD) isconstructed for the studied high-pressure mafic granulite.
3.2. Sillimanite–garnet gneiss (11YC02-2)
Sample 11YC02-2 (Fig. 3b) is composed of garnet, K-feldspar (ksp),biotite (bi), sillimanite (sill), plagioclase, staurolite (st), quartz andminor ilmenite. Staurolite occurs as anhedral relict crystals in sillimanite.Sillimanite occurs as fibrous crystals in contact with K-feldspar (Fig. 4b),showing a weak preferred orientation parallel to the regional foliation.Sillimanite and plagioclase are most likely to have been produced fromthe following dehydration melting reactions (Lal and Ackermand, 1979;Spear et al., 1999; White et al., 2001; Yardley, 1989):
Therefore, the peak assemblage is characterized by sillimanite + K-feldspar+garnet+plagioclase+biotite+quartz+ ilmenite, for whichthe P–T conditions have been constrained at 7–8 kbar and 750–800 °C(Wu et al., 2009).
3.3. Olivine–diopside marble (11YC05-7)
Marble (11YC05-7, see Fig. 3c) is reported here from a variety ofhigh pressure rocks in the Kongling Complex although as a rathersubordinate lithology. It contains calcite, olivine, with minor diopside
(Fig. 4c). P–T pseudosections calculated with the PERPLE_X computerprogram package (Connolly, 2005) for marble indicate that the P–Trange of the mineral assemblage of calcite + olivine + diopside is10–14 kbar and 800–950 °C (Massonne, 2011).
4. Zircon U–Pb ages and Lu–Hf isotope compositions
One high-pressure mafic granulite (11YC01-6), three garnet–sillimanite gneisses (11YC02-2, 02-8 and 02-11), one olivine–diopsidemarble (11YC05-7) and one garnet-bearing S-type granite (11YC06-1)were collected for zircon U–Pb dating and Hf isotope analyses. Zircongrains were separated from the crushed rock samples using initialheavy liquid and subsequent magnetic separation. Zircon grains werehand-picked, embedded in epoxy resin mounts and polished.
4.1. Analytical techniques
Cathodoluminescence (CL) and electron backscatter (BSE) imageswere taken on polished zircon grains using a JEOL JSM6610-Lv scanningelectron microscope. These images were used in targeting specific partsof the grains. LA-ICPMS work was done at the Jack SatterlyGeochronology Laboratory at the University of Toronto using a VGSeries 2 Plasmaquad ICPMS equipped with a 75 l/s rotary pump on theexpansion chamber (S-option) for enhanced sensitivity, and 213 nmNew Wave laser system. Grains were partially ablated using a 213 nmlaser beam diameter of 10–40 μm at 5–10 Hz and 40% power. Datawere collected on 88Sr (10 ms), 206Pb (30 ms), 207Pb (40 ms), 232Th(10 ms) and 238U (20 ms). Immediately prior to each analysis, thespot was pre-ablated over a larger area than the beam diameter forabout 10 s to clean the surface and remove any surface alteration.Following a 10 s period of baseline accumulation the laser samplingbeam was turned on and data were collected for 35 s followed by a50 s washout period. Instability due to mineral zoning was dampenedthrough the use of a 75 ml mixing chamber in-line with the He flowtransporting the ablated sample to the plasma. Data were edited andreduced using custom VBA software (UTILLAZ program) written byD. Davis. No corrections were made for common Pb, since this shouldbe negligible in unaltered zircon. 88Sr was monitored in order to detectintersection of the beam with zones of alteration or inclusions, orpenetration of the beam through the sample. Pb–U data were rejectedfrom areas with excess 88Sr signal. The Th/U ratio of the zircon, whichcan be a useful petrogenetic indicator, was also measured. Zirconstandards were from sample DD85-17, a quartz diorite from northernOntario dated at 3002 +/− 2 Ma (Tomlinson et al., 2003), and fromsample DD91-1, a monzodiorite from the Pontiac province of Quebecdated at 2682+/−1Ma (Davis, 2002). Sets of 3 sample measurementsare bracketed by measurements on standards. Analytical data are givenin Supplementary Table 1. Concordia diagrams are plotted in Fig. 7 usingthe Isoplot program of Ludwig (2003). 207Pb/206Pb ages are the mostprecise and accurate for U–Pb data in this age range. They are calculatedby fitting the data set to a line forced through the origin of Concordiaand are therefore insensitive to Pb/U errors. Error ellipses andregression errors are given at 95% confidence levels.
Lu–Hf isotopic compositions of zircons were analyzed in situ using aNeptune Plasma ICP-MSwith an Agilent 7500a Q-ICP-MS and a 193nmlaser ablation system at the Institute of Geology and Geophysics(Beijing), Chinese Academy of Sciences. Analytical procedures weredescribed in Xie et al. (2008). Spot laser ablation was adopted in thisstudy with a beam size of 30–40 μm and laser pulse frequency of8–10 Hz, with every five spots being bracketed by standard zircon91500 and GJ-1. The decay constant for 176Lu of 1.865 × 10–11 year−1
(Scherer et al., 2001), and the chondritic ratios of 176Hf/177Hf(=0.282772) and 176Lu/177Hf (=0.0332) as derived by Blichert-Toftand Albarede (1997) are used in this paper. The mantle extractionmodel age (TDMC ) was calculated by projecting the initial 176Hf/177Hfratio of zircon back to the depleted mantle model growth curve,
assuming a 176Lu/177Hf ratio of 0.009 for Archean upper continentalcrust (Martin, 1986; Xia et al., 2006; Zhang et al., 2006c). The Lu–Hfisotope results are presented in Supplementary Table 2.
4.2. Results of zircon U–Pb analyses
4.2.1. Sample 11YC01-6This sample is a high-pressuremafic granulite collected from the top
formation of the Kongling Group (Figs. 2, 3a). CL images show thatzircon grains are rounded and characterized by nebulous sector-zoning (Fig. 6a–b), typical of a metamorphic origin. On the Concordiadiagram (Fig. 7a), a total of forty spot data are all concordant to nearlyconcordant and define an intercept age of 2009±7Ma (MSWD=1.4;Fig. 7a).
4.2.2. Sample 11YC02-2This sample is a graphite–garnet–sillimanite gneiss from the lower-
most formation of the Kongling Group (Figs. 2, 3b). Zircons are subhedralin shape, and show clearly core-rim texture with wide, weakly lumi-nescent, structureless overgrowth surrounding light concentric oscillatory-zoned cores (Fig. 6c–d). The concentric oscillatory-zoned zircon corespossess Th/U ratios of 0.52–0.54,typical of igneous origin; whereas thezircon overgrowth rims possess rather low Th/U ratios ranging from0.003 to 0.08 (90% are lower than 0.01; Supplementary Table 1b),interpreted to be of metamorphic origin. Of the twenty-six data points,two were made on the igneous zircon cores and yielded concordant207Pb/206Pb ages of ~ Ma (Fig. 7b); the other twenty-four on themetamorphic zircons define an intercept age of 2000 ± 7 Ma(MSWD=0.94; Fig. 7b).
4.2.3. Sample 11YC02-8Sample 11YC02-8 is a garnet–sillimanite–staurolite gneiss from the
bottom formation of the Kongling Group (Fig. 2). Zircons separatedfrom this sample are either oscillatory-zoned grains (Fig. 6e) or showcore-rim textures characterized by wide, weakly luminescent, struc-tureless overgrowth surrounding light concentric oscillatory-zonedcores (Fig. 6f). The zircon rims have much lower Th/U ratios (0.006–0.044 except for one at 0.242, Supplementary Table 1c) than those ofoscillatory-zoned single zircon grains and zircon cores (0.58–1.12,Supplementary Table 1c). On the concordia diagram (Figs. 7c), fourspots on oscillatory-zoned single zircon grains and zircon cores yieldedconcordant 207Pb/206Pb ages ranging from 2131 to 2198Ma, interpretedas the magmatic ages of detrital zircons from the sedimentary protolith;the other sixteen on zircon rims define an intercept age of 2004±6Ma(MSWD=1.3), considered to be the metamorphic age.
4.2.4. Sample 11YC02-11This sample is a garnet–sillimanite gneiss from the lowermost
formation of the Kongling Group (Fig. 2). Zircons are subhedral androunded grains with complicated internal textures (Fig. 4g–h) andshow rather low Th/U ratios of 0.006–0.074 (Supplementary Table 1d),typical of a metamorphic origin. A total of forty data points overlap anddefine an intercept age of 2003±5Ma (MSWD=0.88; Fig. 7d).
4.2.5. Sample 11YC05-7Sample 11YC05-7 is an olivine–diopside marble from the uppermost
formation of the Kongling Group (Figs. 2, 3c). Zircons are also subhedraland rounded showing complicated internal textures (Figs. 6i–j) interpretedto be of metamorphic origin. On the concordia plot (Fig. 7e), all twentyanalyses overlap, defining an intercept age at 2001±5Ma (MSWD=0.85).
4.2.6. Sample 11YC06-1This sample is a garnet-bearing S-type granite from the Kongling
Complex (Fig. 2). The outcrop is white, and locally contains darkinclusions (Fig. 3d). The analyzed sample consists mainly of biotite, K-feldspar, garnet, plagioclase and quartz (Fig. 4d). Zircons extracted
Fig. 6.Representative CL images of zircons for samples (a–b) 11YC01-6, (c–d) 11YC02-2, (e–f) 11YC02-8, (g–h) 11YC2-11, (i–j) 11YC05-7 and (k–l) 11YC06-1. See detailed descriptions inthe text.
205C. Yin et al. / Lithos 182–183 (2013) 200–210
from this sample are represented by grains with planar zoning (Fig. 4k)or oscillatory-zoned grains with inherited oscillatory-zoned cores(Fig. 4l), typical of igneous origin. A total of twenty spots were analyzed.On the concordia plot (Fig. 7f), three analyses on inherited zircon coresyielded 206Pb/207Pb ages of 2595–2849 Ma; the other seventeenanalyses overlap, defining an intercept age of 2002±9Ma (MSWD=0.67), interpreted as the emplacement age of the S-type granite.
4.3. Results of Lu–Hf isotope analyses
4.3.1. Metamorphic rocks (samples 11YC01-6, 02-2, 02-8, 02-11and 05-7)The Supplementary Table 2a–e presents the results of Lu–Hf
analyses on detrital zircon and metamorphic zircon from threegarnet–sillimanite gneisses (samples11YC02-2, 02-8 and 02-11), onehigh-pressure mafic granulite (11YC01-6) and one olivine–diopsidemarble (11YC05-7). The detrital zircons (2131–2849Ma) possess nearlyidentical 176Hf/177Hf ratios ranging from 0.281284 to 0.281313,corresponding to negative εHf (t) values ranging from −4.07 to −2.58and Hf model ages (TDMC ) of 2.82–2.85 Ga. Metamorphic zircons havewider ranging 176Hf/177Hf ratios of 0.281027–0.281537, with εHf (t)values of −17.62–1.10 and Hf model ages (TDMC ) of 2.46–3.40Ga.
4.3.2. S-type garnet-bearing granite (11YC06-1)A total of twenty zircons from the S-type garnet-bearing granite
were analyzed for Lu–Hf. Three inherited zircon grains showrelatively homogeneous 176Hf/177Hf ratios of 0.280856–0.281059,with negative εHf (t) values of −5.42 to −3.46 and Hf model ages(TDMC ) of 3.22–3.48 Ga. Analyses on the remaining seventeen grainsshow 176Hf/177Hf ratios of 0.281455–0.281654, which correspond
to εHf (t) values of −1.96 to 5.12 and Hf model ages (TDMC ) of 2.25–2.61Ga (Supplementary Table 2f).
5. Whole-rock Sm–Nd isotopes
5.1. Analytical techniques
Sm–Nd isotope analyses were performed at the Institute of Geologyand Geophysics (Beijing), Chinese Academy of Sciences, using a FinniganMAT 262 multi-collector mass spectrometer. Analytical procedures weredescribed in Qiao (1988). The 143Nd/144Nd ratios were adjusted relativeto the Shin Etsu JNdi-1 standard value of 0.512105. ɛNd was calculatedassuming 143Nd/144Nd = 0.512638 and 147Sm/144Nd = 0.1966 forpresent-day CHUR (Jacobsen andWasserburg, 1980); TDMwas calculatedwith 143Nd/144Nd=0.51315 and 147Sm/144Nd=0.2137 for present-daydepleted mantle (Goldstein et al., 1984).
5.2. Results of Sm–Nd isotope analyses
Sm–Nd isotopic analyses for a high-pressure mafic granulite(11YC01-6) and two garnet–sillimanite gneiss (11YC02-2 and11YC02-8) from the Kongling Group are given in Table 1. The high-pressure mafic granulite possesses an Nd concentration of 9.659 ppmand εNd (2.01 Ga) value of −0.84, which corresponds to an Nd modelage (TDMC ) of 2.53Ga, consistent with the zircon Hf model age (TDMC ) of2.56 Ga. In contrast, the garnet–sillimanite gneiss shows much higherNd concentrations (25.20–41.99 ppm) and lower εNd (2.0 Ga) valuesranging between −5.25 and −4.56, with Nd model ages (TDMC ) of2.82–2.88 Ga, which are again consistent with the zircon Hf modelages (TDMC ) of 2.80–2.82Ga.
3 5 7 9 11 13 15 170.25
0.35
0.45
0.55f) 11YC06-1
Inherited magmaticzircon cores
2595-2849 Ma
Magmatic zirconsintercept at 2002 9 Ma
MSWD = 0.67
5.6 6.0 6.4 6.8 7.25.2 7.6
0.32
0.34
0.36
0.38
0.40
0.42
0.30
0.44 e) 11YC05-7
Metamorphic zirconsintercept at 2001 5 Ma
MSWD = 0.85
Magmatic zircons2244 Ma
Metamorphic zirconsintercept at 2000 7 Ma
MSWD = 0.94
b) 11YC02-2
Metamorphic zirconsintercept at 2009 7 Ma
MSWD = 1.4
a) 11YC01-6
5.4 5.8 6.2 6.6 7.0 7.40.32
0.34
0.36
0.38
0.40
0.42
4.5 5.5 6.5 7.5 8.5
Metamorphic zirconsintercept at 2004 6 Ma
MSWD = 1.3
Inherited magmaticzircon cores
2131-2198 Mac) 11YC02-8
0.30
0.34
0.38
0.42
0.46
5.0 6.0 7.0 8.0 9.0
4.5 5.5 6.5 7.5 8.53.50.30
0.34
0.38
0.42
0.46
0.42
0.46
0.22
0.26
0.30
0.34
0.38
0.50
Metamorphic zirconsintercept at 2003 5 Ma
MSWD = 0.88
d) 11YC02-11
206 P
b/23
8 U20
6 Pb/
238 U
206 P
b/23
8 U
207Pb/235U 207Pb/235U
Fig. 7. Concordia diagram of zircon U–Pb analytical results for samples (a) 11YC01-6, (b) 11YC02-2, (c) 11YC02-8, (d) 11YC02-11, (e) 11YC05-7 and (f) 11YC06-1.
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6. Discussion and implications
6.1. Age of the protoliths of the Kongling Group
Like other Palaeoproterozoic high-grade metamorphic supracrustalrocks in India, North China and North America, the protoliths of themetasedimentary rocks of the Kongling Group are considered to havebeen deposited on a passive continental margin (Condie et al., 1992).Zircons from these metasedimentary rocks previously yielded SHRIMPU–Pb ages varying from 2644 to 3131Ma (Table 2), but the depositionalagewas unknown. Qiu et al. (2000) interpreted that the youngest zircon,of rounded homogeneous morphology and Th/U ratio of 0.6, is ofmetamorphic origin and proposed that the protolith of thesemetasedimentary rocks formed at about 2871 Ma. However, this
Table 1Sm–Nd isotope of representative samples from the Kongling Group with comparison of zircon
conclusion is inconsistent with our new geochronological data. Asshown in Table 2, detrital zircons from paragneiss samples 11YC02-2and 11YC02-8 have U–Pb ages of between 2244 and 2131 Ma. Thissuggests that at least some of the sedimentary protoliths of themetamorphic rocks in the Kongling Group were deposited in thePalaeoproterozoic, at some time after 2131Ma, not Archean as previouslyconsidered, unless the zircons were partially reset by diffusion duringmetamorphism.
6.2. Age and tectonic setting of metamorphism of the Kongling Group
Petrographic evidence indicates that the protoliths of these mafic,pelitic and carbonate-bearing rocks underwent high-pressure granulite-facies metamorphism. This paper for the first time reports a high-
Table 2Summary of zircon U–Pb ages from the Kongling Complex of the Yangtze Block, South China.
Sample no. Rock type Metamorphic zircon Detrital zircon Method Reference
Garnet amphibolite 1891Ma Hb K–Ar Jiang (1987)KH05 Metapelite 1939Ma Sm–Nd Ling et al. (2001)KH35 Garnet amphibolite 1958Ma Sm–Nd Ling et al. (2001)KH40 Metapelite 1933Ma 2871–3130Ma SHRIMP Qiu et al. (2000)KH21 Metapelite 2644–3275Ma SHRIMP Qiu et al. (2000)KH12 Metapelite 1948Ma LA-ICPMS Zhang et al. (2006b)KH38 Metapelite 1979Ma LA-ICPMS Zhang et al. (2006b)KH35 Amphibolite 1943Ma LA-ICPMS Zhang et al. (2006b)06HL21 Metapelite 2003Ma LA-ICPMS Wu et al. (2009)06HL12 Garnet amphibolite 2857Ma LA-ICPMS Wu et al. (2009)06HL30 Garnet amphibolite 2015Ma LA-ICPMS Wu et al. (2009)F5N Granulite-facies BIF 1990Ma LA-ICPMS Cen et al. (2012)11YC01-6 High-pressure mafic granulite LA-ICPMS This study11YC02-2 Graphite–garnet–sillimanite gneiss 2009Ma LA-ICPMS This study11YC02-8 Garnet–sillimanite–staurolite gneiss 2000Ma 2244Ma LA-ICPMS This study11YC02-11 Garnet–sillimanite gneiss 2004Ma 2131–2198Ma LA-ICPMS This study11YC05-7 Olivine–diopside marble 2001Ma LA-ICPMS This study11YC06-1 Garnet-bearing S-type granite 2002Ma 2595–2849Ma LA-ICPMS This study
1950 2000 2050 2100 2150 2200 22500.00
0.02
0.04
0.06
0.08
0.10
0.30
0.50
0.70
0.90
1.1011YC02-2
11YC02-8
11YC02-11
11YC02-2
11YC02-8
Fig. 8. Distribution of Palaeoproterozoic U–Pb ages and their Th/U ratios for igneous andmetamorphic zircons from the Kongling Group.
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pressure mafic granulite (sample 11YC01-6), whose mineral assemblageand P–T conditions define a clockwise P–T path, suggesting a continent–continent collision tectonic setting. This tectonic model is consistentwith the tectonothermal evolution of the metasedimentary rocks,including the olivine–diopside marbles, in the Kongling Group becauseonly subduction and collision could bring the sedimentary precursors ofthe pelitic gneiss and marbles to a deep enough crustal level for high-pressure granulite-facies metamorphism (O'Brien and Rötzler, 2003).Previous geochronological data revealed a wide metamorphic age rangeof 1891–2015Ma (see Table 2). In addition, few of these metamorphicages were supported by reliable isotopic data, Th/U ratios and CL imagesof metamorphic zircons from the three types of metamorphic rocks. Inthis study, CL images have shown two types of metamorphic zirconsfrom the Kongling Group. The first type occurs as simple euhedral grainswith chaotic internal textures or complicated internal textures (Fig. 6a, b,g, h, i, j), whereas the second type occurs as overgrowth rims surroundingdetrital zircon cores of igneous origin (Fig. 6c, d, f). Although meta-morphic zircons from mafic granulite and marble have high Th/U ratios,metamorphic zircons of metasedimentary rocks are characterized bymuch lower Th/U ratios (95% lower than 0.02), compared to magmaticzircon cores or single magmatic detrital zircons (Fig. 8). As listed inTable 2, these metamorphic zircons from samples 11YC01-6, 11YC02-2,11YC02-8, 11YC02-11 and 11YC05-7 yield consistent ages of 2009 ±7 Ma, 2000 ± 7 Ma, 2004 ± 6 Ma, 2003 ± 5 Ma and 2001 ± 5 Ma,respectively. This is also consistent with the age of 2002±9Ma obtainedfor the garnet-bearing S-type granite (11YC06-1) in the KonglingComplex. Generally, S-type granites are considered to be the products ofpartial melting of metapelites at shallow levels during the synorogenicstage and are abundant in many orogenic belts related to continentalcollision (Barbarin, 1990, 1999; Bonin, 1990; Lameyre, 1988; Yin et al.,2009). All six ages overlap within error and define an average of2003 +/− 2 Ma (MSWD = 0.9) for regional high-pressure granulite-facies metamorphism of the Kongling Group. This metamorphic event isalso recorded at ~2.0 Ga by the TTG gneisses of the Kongling Complex(Chen et al., 2013a,b; Gao et al., 2011; Qiu et al., 2000; Zhang et al., 2006a).
6.3. Crustal evolution of the Kongling Complex
The Kongling Complex contains the only known Archean rocks andthe oldest detrital zircons in South China (Gao et al., 1999, 2001; Jiaoet al., 2009; Qiu et al., 2000; Zhang et al., 2006b). Consequently, theirgenesis and evolution are of extraordinary significance for under-standing the timing of crustal extraction and reworking. Previousstudies suggest that the Kongling Complex underwent at least threeepisodes of Archean crustal growth at 3.3–3.2 Ga,~2.9 Ga and 2.7–2.6 Ga, respectively (Gao et al., 2011; Jiao et al., 2009; Qiu et al., 2000;
Zhang et al., 2006a). No Palaeoproterozoic crustal event had beenrecognized in the Kongling Complex until this study. In this paper, wehave for the first time reported the presence of Palaeoproterozoicdetrital zircons (2131–2244 Ma) from metasedimentary rocks in theKongling Complex. These Palaeoproterozoic detrital zircons possessnegative εHf (t) values ranging from −4.07 to −2.58 and Hf modelages (TDMC ) of 2.82–2.85 Ga. In addition, a short-lived metamorphicevent that includes S-type granite plutonism has been precisely datedat 2003+/− 2Ma. Metamorphic zircon has nearly identical or slightlyhigher 176Hf/177Hf ratios compared to detrital zircon cores, indicatingthat most of the metamorphic zircons resulted from recycling of oldermagmatic zircon, with a small addition of extra hafnium from thematrix during the process (Gerdes and Zeh, 2009; Sun et al., 2002; Wuet al., 2007; Yin et al., 2011, 2013; Zeh et al., 2007, 2010). Somemagmatic zircons from the S-type granite contain older inherited zirconcores of 2595–2849Ma, which possess εHf (t) values of−5.42 to−3.46and Hf model ages (TDMC ) of 3.22–3.48Ga.
The detrital and metamorphic zircons from the metasedimentaryrocks and the magmatic zircons from the S-type granite all showconsistent hafnium depleted model ages (TDMC ). The lowest εHf(t)values of these zircons define an evolution line that intersects thedepleted mantle line at about 3.5 Ga (Fig. 9). This suggests that theoldest juvenile material was extracted from the depleted mantle at~3.5Ga. However, 98% of zircon hafnium data scatter between 2.2 and2.9 Ga (Fig. 9), which is consistent with whole-rock neodymium
11YC01-6
11YC02-11
11YC05-7
11YC02-2
11YC02-8
11YC05-5
DM
176 Lu/177 Hf=0.009
3.5 Ga
CHUR
2.2 Ga
2.9 Ga
Fig. 9. Composite plots of εHf (t) values vs. ages (Ga) for the analyzed zircons from allsamples. The depleted mantle trend (DM) was constructed using the modern-day valuesof mid-ocean ridge basalts (MORB) of Blichert-Toft and Albarede (1997) (176Hf/177Hf =0.282772 and 176Lu/177Hf = 0.0332), and the decay constant for 176Lu of 1.865 × 1011
(Scherer et al., 2001).
208 C. Yin et al. / Lithos 182–183 (2013) 200–210
model ages (TDMC ) of 2.53–2.88 Ga (Table 1). One of the most likelyinterpretations is that there was a 2.9Ga crust in the Kongling Complex,and that this crust was reworked to form the protoliths of the meta-sedimentary rocks in the period 2.1–2.2Ga, with little or no addition ofjuvenile mantle material. The protoliths of the metasedimentary rocksthen experienced granulite-facies metamorphism at ~2.0 Ga. Thisprovides additional evidence that the S-type granites are derived frompartial melting (reworking) of the protoliths of metapelites at ~2.0 Ga.Therefore, these zircons might record a significant Palaeoproterozoiccrustal reworking event of Archean crust materials in the KonglingComplex.
6.4. Tectonic evolution of the Kongling Complex
New zircon U–Pb data reported here constrain the maximumdepositional age of the Kongling Group at 2131Ma (age of the youngestdetrital zircon), while metamorphic zircons yield consistent agesbetween 2009 and 2000 Ma. Thus, the sedimentary protoliths of theKongling Group must have been deposited in a period between 2.1and 2.0 Ga. Petrographic evidence suggests that high-pressure maficgranulite experienced a peak metamorphic stage (M1) at N12 kbarand N870 °C, and a subsequent decomposition stage (M2) at b9 kbarand b850°C. Thesemineral assemblages and their P–T conditions definea clockwise P–T path involving near-isothermal decompression (Fig. 5).This suggests that the Kongling Group was involved in continentalsubduction and/or collision. Therefore, the high-pressure maficgranulites reported in this study and the reconstructed P–T pathindicate that the Kongling Group represents a Palaeoproterozoiccontinent–continent collisional belt at ~2.0 Ga. Taken together, newpetrographic evidence, zircon U–Pb ages and Hf isotopic data andwhole-rock Nd isotopic data presented in this study enable us topropose the following preliminary scenario for the tectonic evolutionof the Kongling Complex in South China:
(1) At 2.1–2.0 Ga, the sedimentary protolith of the Kongling Groupwas deposited on a passive continentalmargin, above a basementconsisting of Archean TTG gneisses of the Kongling Complex.
(2) At ~2.0 Ga, the sedimentary rocks and the passive continentalmargin were subducted beneath an active continental margin,leading to continent–continent collision. The collision resulted ingranulite facies metamorphism of the sedimentary rocks andmafic rocks at lower crustal levels. Meanwhile and shortly later,migmatization of the TTG gneiss, the basement of the Kongling
Complex, occurred and syn-collisional S-type granites were locallyemplaced, probably due to partial melting of the sedimentaryrocks.
(3) At ~1.85 Ga, possibly due to delamination of orogenic root, theKongling Complex experienced post-collisional extension withwidespread emplacement of mafic dykes (Peng et al., 2009) andQuanyishang high-K A-type granite (Peng et al., 2012; Xionget al., 2008).
6.5. Implications for reconstruction of Columbia
Although the configurations of the supercontinents Gondwana andPangea are relatively well constrained (Veevers, 2004), those of theolder supercontinents Rodinia and Columbia are still debated. Inparticular, the position of the South China in these supercontinentreconstructions remains controversial (Cawood et al., 2013; Evans,2009; Li et al., 2008; Wu et al., 2012; Yu et al., 2008; Zhang et al., 2012a,b,c; Zhao et al., 2002). For instance, some researchers proposed that theSouth China occupied an intracratonic position between Australia andLaurentia (Li et al., 2008), whereas others argued that it was either onthe margin of Rodinia near Australia (Zhao and Cawood, 1999; Zhouet al., 2002) or connected with northwestern Australia and remotenortheastern India (Yang et al., 2004). Most recently, Cawood et al.(2013) proposed that the South China was assembled and thenmaintained a position off Western Australia and northeast India fromNeoproterozoic to Palaeozoic along the periphery of both the Rodiniaand Gondwana supercontinents. Although the location of the SouthChina relative to other microcontinents in Rodinia is still a contentiousissue, it has now become increasingly clear that the South China was animportant component of Rodinia. In contrast, it remains unknown orcontroversial whether the South China was part of the Palaeo- toMesoproterozoic supercontinent Columbia and, if so, where it waslocated within this supercontinent (Evans, 2009; Zhang et al., 2012a,b,c;Zhao et al., 2002). Themain reason for this controversy, and the resultinguncertain positions of the South China Craton in Columbia re-constructions, is that no 2.1–1.8 Ga orogen or mobile belt had beenidentified in South China. In this paper, we provide evidence that the~2.0 Ga collision is of continent–continent type, followed by ~1.85 Gapost-collisional extension based on petrography, zircon U–Pb ages andHf isotopic data, and whole-rock Nd isotopic data of high pressuremafic granulites, metasedimentary rocks and high-grade marble fromthe Kongling Complex of the Yangtze Block, South China. This 2.0–1.85 Ga tectonic evolution was coincident with global-scale collisionalevents in the period, such as the 1.95–1.85 Ga Khondalite Belt and theTrans-North China Orogen in North China (see Fig. 1), the 2.0–1.9 GaCapricorn Belt in Western Australia, the 2.0–1.9 Ga Limpopo Belt inSouth Africa, the 2.1–2.0 Ga Transamazonian and Eburnean Orogens inSouth America and West Africa, the 1.95–1.85Ga Trans-Hudson Orogenand its equivalents (Taltson–Thelon, Wopmay, New Quebec, Foxe,Makkovik, Ungava and Torngat Orogens) in North America, and the1.9–1.8Ga Nagssugtoqidian Orogen in Greenland, Kola–Karelia, Volhyn–Central Russian and Pachelma Orogens in Baltica (including EastEurope) and Akitkan Orogen in Siberia (Zhao et al., 2002 and referencestherein). These collisional events led to the assembly of the Palaeo-Mesoproterozoic supercontinent (Zhao et al., 2002), called “Nuna”(Hoffman, 1997), “Hudson” (Zhao et al., 2000), “Columbia” (Rogers andSantosh, 2002), or “Hudsonland” (Pesonen et al., 2003). Therefore, theresults of this study provide important evidence that the Yangtze Blockin South China was one of the components of the Palaeo-Mesoproterozoic supercontinent (Zhao et al., 2002, 2004).
Acknowledgements
This research was financed by an NSERC grant, a China GeologicalSurvey grant (1212011121116) and a China NSFC grant (40725009).We thank M. Munteanu and an anonymous reviewer for their
209C. Yin et al. / Lithos 182–183 (2013) 200–210
comprehensive and constructive comments. M. Scambelluri is thankedfor editorial assistance and constructive reviews. Profs. Jianping Zhengand Junhong Zhao are gratefully thanked for help in the field. Dr.Yueheng Yang, Fu Liu, Ruojuan Wang and Min Qu from ChineseAcademy of Sciences are thanked for their help in zircon Lu–Hf isotopicanalysis.
Appendix A. Supplementary data
Supplementary data to this article can be found online at http://dx.doi.org/10.1016/j.lithos.2013.10.012.
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