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Journal of EaPrinted in ChiDOI: 10.1007/
Ding, R. X., Guangxi Area
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Zou, H. P., Ma, China. Journa
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Ruxin Ding
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BSTRACT: Thangtze and Catrobablycrosses ndstone sample Archeozoic ahich are coevaported in the Pour detrital zie more inclineg the Sinian-Crzoic. But if tht between Guilsouthwestern
etrital zircons wital zircons witEYWORDS: C
UCTION hina Block, onesia Block in the hough the formanding Precambnd the boundary
are yet to be de scholars presePaleozoic betw
est of South Chieastern Guangxal., 2015), oth
dual oceanic baSouth China Blo
ng author: adszh yinf.k
versity of Geosc017
ceived Octoberccepted April 13
Vol. 28, No. 2
723-y
Min, K., et al., al of Earth Scie
rcon U-ata in th
1, 2, HepingXux
rth Science and ncial Key Laboartment of Geol
4. Exploratiitute of Geologyorcid.org/0000-
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he Eastern Guathaysia blocks,there. We det
les in the Siniaand Neoproter
al to the GrenvPrecambrian sircons are likeled to accept th
Cambrian periohe timing of colin-Yongfu fausedimentation
with ages of ~5th over 3 000 MCathaysia Bloc
e of major blocsoutheast and Y
mation of South brian tectonics oy location in thedisputed (Shu, ent that there waween Cathaysia ina Block throuxi area (Qin et
hers scholars puasin at the end oock (He et al., 20
hp@mail.sysu.ektnf@sinopec.cciences and Spr
r 2, 2015. 3, 2016.
2, p. 295–304,
2017. Detrital ence, 28(2): 295
-Pb Geohe Easte
g Zou *1, 2, Kxuan Ma5, Zh
Geological Engratory of Minerlogical Scienceon Branch Comy, Chinese Acad-0002-1174-519Yin: http://orci
angxi area loca, which is an imtermined LA-Ian-Cambrian srozoic, with thvillian magmatstrata of the adly derived frome opinion thatod in Eastern Gllision is the E
ultand Lipu faun boundary of 590 Ma which Ma U-Pb ages wck, Yangtze Blo
cks in East AsiaYangtze Block iChina Block is of China, the tie southwest of S
2012; Zhao, 2as a residual ocand Yangtze b
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Zircon U-Pb G5–304. doi:10.1
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ates in the soutmportant regioICPMS U-Pb astrata in this rhree notable ctic activity. Th
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Early Paleozoicult) beyond thef Cathaysia Bloprobably sourwhich record tock, eastern Gu
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thwestern parton because theages for detritregion. The resconcentrates ahe new age dis
western Cathayia Block. Comt an ocean basif the timing o
c, we conclude e west of Dayaock and Yangt
rced from nortthe early formauangxi area, de
In this researcmples in the Day
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GEOLOGICAThe study are
haysia Block ag. 1). The Yangall amount of ges of 3 200–2
et al., 2000; Geentree and Li, ensively distribu
around the ma0a; Zheng et al.9). The Cathayely Mid-Paleop
mposed dominahu et al., 2011; Y
y of Sinian–Ca17-0723-y. http
f Sinian–Area, Ch
Yin *4, Xiahen1, 2 rsity, Guangzho
Processes, Guanesville, FL 32610041, China Beijing 100037id.org/orcid.org914-5034
t of the transite boundary beal zircons extrsulting ages art 991, 974, an
stribution is siysia Block, sug
mbined with othin between the
of collision is ththat Luzhai u
oshan regoin mtze Block. We theastern Gondation of the earetrital zircon, U
ch, we collectedyaoshan region P-MS U-Pb daw useful evidennic basin existe
border betwe
AL SETTING ea locates betwand the southeagtze basement Achaean TTG900, 2 700–2 4
Gao et al., 19992008) and 1 10
uted Neoproteroargin of the Yan., 2007; Li et alysia basement hproterozoic (1 antly of gneissYu et al., 2010
ISS
ambrian Strata ://en.earth-scien
–Cambhina
aodong Du1,
ou 510275, Chinngzhou 510275,11, USA
7, China g/0000-0002-40
tion zone betwetween two bloracted from thre in the rangend 964 Ma, allimilar to the dggesting that mhers’ research, e two blocks dhe Early Neop
uplift (i.e., the might be one palso get a few
dwana and 13 rth. U-Pb dating.
d Sinian–Cambof Eastern Gua
ating for detritance to test wheed or not, and een Cathaysia
ween the southwastern part of Yconsists of Pro
G rocks with th400 and 2 100–9). There are m00–900 Ma ignozoic (840–740ngtze Block (e.l., 2003b; Zhou has been propo800–2 000 Ma, amphibolite
0). There are ign
SN 1674-487X
in the Easternnce.net
brian
2,
na , China
54-7292
een ocks hree e of l of
data most
we dur-pro-up-
part w of
de-
brian sandstoneangxi area, andal zircons. We
ether the Paleo-further discuss
and Yangtze
western part ofYangtze Blockoterozoic and ahe ages in the1 800 Ma (e.g.,
minor 1 700 Maneous rocks and0 Ma) magmat-g. Wang et al.,et al., 2002; Li
osed to be of aa) origin and isand migmatiteneous rocks in
X
n
e d e -s e
f k a e , a d -, i, a s e
Ruxin Ding, Heping Zou, Kyoungwon Min, Feng Yin, Xiaodong Du, Xuxuan Ma, Zhangxin Su and Wenjie Shen
296
Figure 1. Geological sketch map of the study area and sample locations map. (a) The geological map and sample locations (all of white regions stand for strata
of post Cambrian); (b) the locations of the researched area between Yangtze Block and Cathaysia Block.
the range 1 900–1 700 Ma, 1 400 Ma and 1 000–700 Ma and are mainly distributed in the northeastern (Wuyishan area) and southwestern (Yunkai area) parts of the Cathaysia Block. After the period at ca. 825 Ma, rift basins were formed in South Chi-na Block (Feng et al., 2016; Shu, 2006; Li et al., 2003a, b). The basement rocks of the Yangtze and Cathaysia blocks are un-conformably overlain in turn by the Upper Neoproterozoic– Lower Paleozoic, Devonian–Lower Triassic and Upper Triassic–Lower Jurassic strata (e.g., Wang et al., 2014; Shu et al., 2011; Wan et al., 2010; Yu et al., 2010). During the Later Neoproterozoic (Ediacaran or Sinian)–Cambrian, most of Yangtze Block was covered by carbonate platform system (Xu et al, 2012; Jiang et al., 2011); meanwhile the Cathaysia Block was broken up into three sub-blocks, namely, the Wuyi, South Jiangxi-Nanling and Yunkai, which were separated from one another by intracontinental rift zones (Yao et al., 2011; Shu, 2006). The intracontinental rift basins in the Cathaysia Block were mainly covered by clastic rocks (Zhou et al., 2016; Shu, 2006; Guangdong BGMR, 1988; Hunan BGMR, 1988; Gua-ngxi BGMR, 1985; Jiangxi BGMR, 1985).
The exposed strata of this study area are Sinian –Cambrian, Devonian–Permian, Jurassic, Cretaceous and Pa-leogene sequences. The Sinian–Cambrian strata are conforma-ble in sequence and composed mainly of clastic rocks. The pre-Devonian and Devonian strata present unconformable con-
tact, the Devonian and Carboniferous strata present conforma-ble contact, the Carboniferous and Permian strata present con-formable or parallel unconformable contact (Yin, 1997). The Jurassic, Cretaceous and Paleogene strata, corresponding to terrestrial facies, are sporadically scattered in the study area. Most of the granitic plutons in the study area were emplaced during Yanshanian periods and few of them were emplaced during Indosinian or Caledonian. The Sinian–Cambrian and Devonian–Permian strata occurred regional folding. In the researched area, the fault strike is mainly NNE-NE with partial NW or close to SN. The fault experienced the multiphased overprinting.
2 SAMPLING
Figure 1 shows sampling locations. Figure 2 shows field pictures of sample locations and photomicrographs of samples. Sample 712-10 (N24°54.487′, E112°01.292′) is col-lected from a meta-siltstone layer in the Sinian stratum in Mashi Town, Jianghua County, Hunan Province. Sample 802-1 (N23°45.257′, E110°39.170′) from the Cambrian sand-stone is taken from near the national highway 321 in Dongrong Town, Teng County, Guangxi Province. Sample 802-6 (N24°06.195′, E110°35.490′) is a Cambrian sandstone near the national highway 321, ~500 m in the north of Hua-ngcun town, Mengshan County, Guangxi Province.
Detrital Zircon U-Pb Geochronologyof Sinian–Cambrian Strata in the Eastern Guangxi Area, China
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Figure 2. Field pictures of sample locations (left) and photomicrographs of samples (right).
3 ANALYTICAL PROCEDURES
We followed a standard mineral separation procedure in-cluding crushing, hand washing, magnetic separation, sepa-rated by alcohol or heavy liquid, selection under microscope, then random selection of zircon grains under binocular, stick-ing grains into target and fixing it by epoxy resin, polishing it by polish plate. The selected zircon grains were examined with JXA-8100 EPMA and each grain’s CL (cathodolumi-nescence) images were taken. In-situ U-Pb dating was con-ducted using Agilent 7500a LA-ICPMS with a laser ablation system of GeoLas 2005. The diameter of the laser beam spot is 32 μm. The external standard sample of element content adopts NIST SRM 610 and the internal standard adopts 29Si. The isotope ratios standard sample adopts 91500 and GJ-1. In the dating process, 5 to 6 zircon grains are dated every 91500 dating twice. The original data were processed by ICPMSDa-taCal (Liu et al., 2008). The U-Pb concordia diagram was generated using Isoplot 3.75 (Ludwig, 2012). The U-Pb dating
were performed at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geos-ciences (Wuhan). 4 RESULTS
In this study, we examined internal structures of 110 zircons for Sample 712-10, 106 zircons for Sample 802-1 and 113 zircons for Sample 802-6. Most of these zircons are hy-pidiomorphic to idiomorphic with linear dimensions of 50–260 μm (sample 712-10), 100–300 μm (802-1), and 100–400 μm (802-6), respectively. Zircon grains are colorless to light pink and are euhedral tosubhedral crystals or crystal fragments. A few grains are subrounded to rounded crystals with pitted surfaces (Fig. 3). The euhedral-subhedral grains suggest little sedimentary transport, whereas the rounded grains suggest input of material that underwent prolonged and possibly multicycle transport. Most of the zircons have clear evidence of oscillatory zoning (Fig. 3). It is generally
Ruxin Ding, Heping Zou, Kyoungwon Min, Feng Yin, Xiaodong Du, Xuxuan Ma, Zhangxin Su and Wenjie Shen
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Figure 3. Representative CL images. Circles stand for the analysis spots and numbers stand for U-Pb ages (Ma). (a), (b), (c) stand for sample 712-10, 802-1,
802-6, respectively.
Detrital Zircon U-Pb Geochronologyof Sinian–Cambrian Strata in the Eastern Guangxi Area, China
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considered that Th/U ratio for the magmatic zircon is greater than 0.2 whereas the metamorphic zircons have Th/U ratios of <0.10 (Rubatto, 2002; Hoskin and Schaltegger, 2003). The majority of our grains yielded Th/U greater than 0.2, indicat-ing a magmatic origin.
Most of the U-Pb ages are concordant (Fig. 4). Because 207Pb/206Pb ages are commonly considered to be more reliable than 206Pb/238U ages for older zircons with the age of more than 1 000 Ma (Compston et al., 1992), 207Pb/206Pb ages for samples are used. For young grains with 206U/238Pb ages<1 000 Ma, we used their 206U/238Pb ages for further discussion.
Figure 4. The 207Pb/235U–206Pb/238U concordia plots.
Figure 5 shows the U-Pb age distributions for three sam-ples. The U-Pb ages are concentrated in four groups: 514–618, 631–1 278, 1 306–2 047, 2 131–2 886 and >3000 Ma. The three samples yield three most prominent peaks at 991, 964 and 974 Ma. The age pattern corresponds to the timing of Grenvil-lian magmatic activities, and possibly marked the formation of Rodinia supercontinent (Li et al., 2008). The period of 514–618 Ma can correspond to Pan-Africa movement and 1 306–2 047 Ma roughly correspond to the formation of Columbia super-continent (Zhao et al., 2004; Rogers and Santosh, 2009). The age group of 2 131–2 886 Ma is probably related to the forma-tion of the Kenorland supercontinent (Pesonen et al, 2003). The oldest age group (>3 000 Ma) is composed of relatively small number of zircons, but they recorded the early formation of the Earth.
5 DISCUSSIONS 5.1 The Identification of Provenance Areas
To identify provenances of the Sinian–Cambrian strata, we compared the new zircon ages with published geochronologic data from the nearby areas, including the Precambrian strata of southeastern Yangtze Block and southwestern Cathaysia Block (Fig. 5). The U-Pb ages obtained from detrital zircons in the Neoproterozoic sedimentary rocks of southeastern Yangtze Block concentrate on Jinningian Period (ca. 800 Ma). The age peak is at 819 Ma, which is within the range reported from various rocks in Yangtze Block (800–850 Ma; Wang et al., 2010a). This period corresponds to the breakup of the Rodinia continent (Li et al., 2003a, b). The U-Pb ages of the detrital zircons in the Neoproterozoic sedimentary rocks of southwes-tern Cathaysia Block are grouped on the Grenvillian Period (ca. 1000 Ma), with the peak at 956 Ma. This suggests that a large scale magmatic activity occurred in Cathaysia Block in the Grenvillian Period, or Cathaysia Block was very close to a Grenvillian orogen (Wang et al, 2008). In fact, recent study showed that granitic gneisses from the Wuyi-Yunkai domain in Cathaysia Block gave zircon U-Pb ages of 985–913 Ma, indi-cating the presence of the Early Neoproterozoic granitic mag-matism in the Cathaysia interior (Wang et al., 2014).
The morphological characteristics of most of our analyzed detrital zircons from the Sinian–Cambrian sandstone samples favor a shorter transport distance. In addition, the paleocurrent data of lower Paleozoic strata in South China Block showed a W‐NNW orientated transport direction from Cathaysia Block across to the central Yangtze Block (Wang et al, 2010b). These data suggest that the source lay to the southeast, either within the southeastern Cathaysia Block or beyond the current margins of the block. Since numerous Paleoproterozoic and Neoprote-rozoic igneous rocks exposed in the Wuyishan and Yunkaida-shan domains of Cathaysia Block (e.g., Li et al., 2014; Wang et al., 2014; Wan et al., 2010, 2007; Shu, et al., 2008), Cathaysia Block is of a suitable age to supply the Paleoproterozoic and Neoproterozoic grains of the analyzed Sinian–Cambrian sam-ples.
In Cathaysia Block, there are age distributions from Arc-heozoic to Neoproterozoic Period and peaks around 1 700–1 800 Ma and 2 500 Ma. This phenomenon shows that magmatic thermal events occurred in the same period and were
Ruxin Ding, Heping Zou, Kyoungwon Min, Feng Yin, Xiaodong Du, Xuxuan Ma, Zhangxin Su and Wenjie Shen
300
recorded by Yangtze Block. The Sinian–Cambrian strata of Yangtze Block are mainly composed of carbonates but those of Cathaysia Block are mainly composed of clastic rocks. This means that detritus could not extend readily across the margin of Yangtze Block because of the intervening carbonate plat-form.
Until now, igneous rocks with ages of ~2 490 Ma and ~590 Ma have not yet been found in Cathaysia Block. However, there are metavolcanic rocks which chemically fall into tra-chyandesitic and rhyolitic sections with U-Pb zircon age of 527 Ma existed in Tunchang, Hainan Island (Ding et al., 2002). The ages of 537 Ma to 507 Ma found in Guzhai pluton located in eastern Guangdong province are interpreted as the Cambrian magmatic event (Ding et al., 2005). Also, Chen et al. (2009) argued for the existence of a magmatic or thermal event exis-tent in South China Block during the Cambrian time (ca. 526 Ma). On the other hand, according to geochemical, provenance,
and paleontological data, it was suggested that during the Neo-proterozoic and Early Paleozoic, South China Block lay along the northern margin of Gondwana (Zhao and Cawood, 2012). Recent work of provenance data in combination with general geological information has suggested that South China Block was located at the nexus between India, Antarctica, and Aus-tralia, along the northern margin of East Gondwana during the Cambrian (Xu et al., 2013, 2014; Cawood et al., 2013), so a few of our detrital zircons with ages of ~2 500 Ma and ~590 Ma probably came from this portion of northeast Gondwana.
Therefore, the main evidence to identify the provenances of Sinian–Cambrian sedimentary rocks is which provides the ages of the detrital zircons, Grenvillian Period (ca. 1 000 Ma) or Jinning Period (ca. 800 Ma). It is apparently shown that the U-Pb ages of the three sample detrital zircons are consistent with the ages of the detrital zircons in the Precambrian strata of southwestern Cathaysia Block. This shows that most of the
Figure 5. The comparison between the U-Pb age patterns of the detrital zircon in this study and the published data in southeastern Yangtze Block and south-
western Cathaysia Block. (a), (b), (c) are the U-Pb age patterns of 712-10, 802-1 and 802-6, respectively; (d) is the U-Pb age pattern of total our three samples;
(e) and (f) are the U-Pb age patterns of southeastern Yangtze Block and southwestern Cathaysia Block, respectively. The age data of the southeastern Yangtze
Block is from Wang et al. (2012, 2010a), Wang and Zhou (2012). The age data of the southwestern Cathaysia Block is from Yu et al. (2010, 2008), Wang et al.
(2008).
Detrital Zircon U-Pb Geochronologyof Sinian–Cambrian Strata in the Eastern Guangxi Area, China
301
Figure 6. The isopach map of the Nanhua–Cambrian strata in Eastern Guangxi area.
detrital zircons in our three samples probably come from the Cathaysia Block, and a few of the detrital zircons with ages of ~2 500 and ~590 Ma probably have some relationship with Gondwana. 5.2 Constraints on the Yangtze-Cathaysian Boundary
We acquire the Nanhua–Cambrian overall thickness con-tour map (Fig. 6) by Kriging interpolation based on the many locations’ thickness measurement (Chen et al., 2006). Seen from the figure, there are two sedimentary centers which sedi-mentary thicknesses are up to 4 000 m, even 6 000 m.
One sedimentary center locates to the north of Guilin- Yongfu faultwhere sediments are mainly carbonate rocks. By this center, the samples from Nanhua stratum by Wang and Zhou (2012) and Sinian–Cambrian stratum by Wang et al. (2013) have shown their provenances are from Yangtze Block. The other sedimentary center locates to the south of Lipu fault where sediments are mainly clastic rocks (Chen et al., 2006). Our samples locate by this clastic sedimentary center, which shows their provenance is Cathaysia Block. In addition, Wang et al. (2013) acquired some samples from the Sinian–Cambrian stratum in Jinjiling Mountain which also shows sediments come from the Cathaysia Block.
Based on the thickness contour map and all the samples’ locations relatively arranging on both sides, we present that Luzhai uplift (i.e., the uplift between Guilin-Yongfu fault and Lipu fault and with few Nanhua–Cambrian sediment) is a very important area. If the timing of collision is the Early Neopro-terzoic, we are more inclined to accept the opinion that there was not an ocean basin between the two blocks during the Sinian–Cambrian Period (Shu, 2012, 2006; Wang et al., 2010b).
But if the timing of collision is the Early Paleozoic (e.g., Qin et al., 2015), we can say that Luzhai uplift beyond the west of Dayaoshan region might be one part of southwestern sedimen-tation boundary of Cathaysia Block and Yangtze Block.
5.3 Identification of Old Zircons (>3 000 Ma)
Among the 328 zircon grains in this study, thirteen yielded U-Pb ages of older than 3 000 Ma (Appendix Table 1). They have (1) Th/U ratios are between 0.17 and 0.78, and (2) oscil-latory zones suggesting the magmatic origin of these zircon grains.
Twelve ages (between 3 018–3 639 Ma) with over 90% concordance are selected for statistical analysis (Fig. 7a) with those published U-Pb age data over 3 000 Ma of detrital zircons from the Cambrian and Precambrian strata in Cathaysia Block (Wang P M et al., 2012; Li et al., 2009;Yu et al., 2008, 2007; Wan et al., 2007). The results show a very weak supply be-tween 3 000–3 300 Ma (Fig. 7a). We also analyzed statistically (Fig. 7b) the published U-Pb age data over 3 000 Ma of detrital zircons from the Cambrian and Precambrian strata in Yangtze Block (Chen et al., 2013; Wang L J et al., 2012; Xiao, 2012; Gao et al., 2011; Zhao et al., 2010; Jiao et al., 2009; Liu et al., 2006; Zhang et al., 2006), the results show a cluster of 3200–3300 Ma (Fig. 7b). Furthermore, the published U-Pb age data over 3 000 Ma of detrital zircons from Permian and older strata in South China Block (Chen et al., 2013; Li et al., 2012, 2009; Wang P M et al., 2012; Wang L J et al., 2012; Wang Y J et al., 2010; Xiao, 2012; Xu et al., 2012; Yao et al., 2012, 2011; Gao et al., 2011; Xiang and Shu, 2010; Zhao et al., 2010; Jiao et al., 2009; Yu et al., 2008, 2007; Wan et al., 2007; Liu et al., 2006; Zhang et al., 2006), the results also shows a cluster of
Ruxin Ding, Heping Zou, Kyoungwon Min, Feng Yin, Xiaodong Du, Xuxuan Ma, Zhangxin Su and Wenjie Shen
302
3 200–3 300 Ma (Fig. 7c). All of the three results show that there maybe occurred some magmatic thermal events before 3 000 Ma. The summit period maybe is between 3 200–3 300 Ma. As mentioned before, most of the detrital zircons in our three samples probably come from Cathaysia Block. However, we cannot make sure that the magmatic thermal events before 3 000 Ma occurred in Cathaysia Block since the grains might be repeatedly transported or transported from an exotic Arc-hean continent (probably from Gondwana).
6 CONCLUSIONS
(1) The detrital zircons LA-ICPMS U-Pb age spectrum of 3 Sinian–Cambrian sandstone samples in the Eastern Guangxi area have the most notable age summits being 991, 974, and 964 Ma. These summits are similar to the summit of detrital zir-cons U-Pb age in the Precambrian strata of the adjacent southwest Cathaysia Block, which means most of the studied three sample detrital zircons probably come from Cathaysia Block.
(2) We are more inclined to accept the opinion that there was not an ocean basin between the two blocks during the
Figure 7. The pattern for detrital zircon U-Pb ages of over 3 000 Ma from
the Cathaysia (a), Yangtze (b) and South China Block (c), respectively
(a)U-Pb age data over 3 000 Ma distribution of detrital zircons from the
Cambrian and Precambrian strata in Cathaysia Block; (b)U-Pb age data over
3 000 Ma distribution of detrital zircons from the Cambrian and Precam-
brian strata in Yangtze Block; (c) U-Pb age data over 3 000 Ma distribution
of detrital zircons from the Permian and earlier strata in South China Block.
Sinian–Cambrian period if the timing of collision is the Early Neoproterzoic. But if the timing of collision is the Early Pa-leozoic, we present that Luzhai uplift beyond the west of Dayaoshan regionmight be one part of southwestern sedimen-tation boundary of Cathaysia Block and Yangtze Block.
(3) We get 13 detrital zircons acquired with over 3 000 Ma U-Pb ages. This shows that there occurred some magmatic thermal events before 3 000 Ma. Combining with the former studies we think the summit of these thermal events maybe is ca. 3 200–3 300 Ma. But we cannot make sure that the mag-matic thermal events before 3 000 Ma occurred in Cathaysia Block since the grains might be repeatedly transported or transported from an exotic Archean continent.
ACKNOWLEDGMENTS
This study was jointly supported by the National Natural Science Foundation of China (No. 41102131), the Fundamental Research Funds for the Central Universities of China (No. 12lgpy22), Guangdong Natural Science Foundation (No. 2015A030313193), China Geological Survey (No. 1212011121064), Chinese Association for science and technology project (No. 2014XSJLW01-02) and China Scholarship Council. We are grateful to Shi’ai Chen, Miaoji Lao and Gang Yang for their assistance in field work. The final publication is available at Sprin-ger via http://dx.doi.org/10.1007/s12583-017-0723-y. Electronic Supplementary Material: Supplementary material (Appendix Table 1) is available in the online version of this article at http://dx.doi.org/10.1007/s12583-017-0723-y. REFERENCES CITED
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