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Geochronology, geochemistry, and tectonic implications of Upper Silurian-Lower
2
Devonian meta-sedimentary rocks from the Jiangyu Group in eastern Jilin
3
Province, NE China
4 5
Zuo-Zhen Hana,b,c*, Hui Liua,b, Zhi-Gang Songa,b, Wen-Jian Zhonga,b, Chao Hana,b, Mei
6
Hana,b, Qing-Xiang Dua,b, Li-Hua Gaoa,b, Jing-Jing Lia,b and Jun-Lei Yana,b
7
a
8
Technology, Qingdao 266590, China
9
b
College of Earth Science and Engineering, Shandong University of Science and
Key Laboratory of Depositional Mineralization & Sedimentary Mineral of Shandong
10
Province, Shandong University of Science and Technology, Qingdao 266590, China
11
c
12
Science and Technology, Qingdao 266237, China
Laboratory for Marine Mineral Resources, Qingdao National Laboratory for Marine
13 14
*Corresponding author: Zuo-Zhen Han
15
College of Earth Science and Engineering, Shandong University of Science and
16
Technology, Qingdao, 266590, China
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E-mail:
[email protected]
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Abstract
24
In this study, we present detrital zircon U-Pb ages and Hf isotopic data and whole-rock
25
geochemical data from meta-sedimentary rocks of the Jiangyu Group in eastern Jilin
26
Province (NE China) to constrain the late Silurian-Early Devonian tectonic evolution of
27
the
28
meta-sedimentary rocks from the Jiangyu Group yielded concordant ages ranging from
29
2926 Ma to 415 Ma, and the youngest zircon populations of the two samples yielded
30
weighted mean ages of 427±3 Ma and 426±3 Ma, respectively. Combined with
31
reliable published muscovite
32
metamorphic ophiolitic mélange, these data indicate that the protoliths of the Jiangyu
33
Group were deposited during the late Silurian-Early Devonian Era. A comparison of the
34
U-Pb ages and Hf isotopic data for detrital zircons from northeastern Gondwana and the
35
Jiangyu Group indicates a probable tectonic affinity. The whole-rock geochemical data
36
indicate that the protoliths of the meta-sedimentary rocks from the Jiangyu Group were
37
graywackes deposited in a continental arc setting. Based on the recognition of the early
38
to middle Paleozoic subduction-accretion events along the eastern segment of the
39
northern margin of the North China Craton (NCC), we infer that the
40
subduction-accretion events may have occurred in the Yanbian area followed by one or
41
more arc-continent collisions after the Early Devonian.
42
Keywords: Zircon geochronology, Geochemistry, Detrital zircons, Jiangyu Group,
43
Xing’an-Mongolia Orogenic Belt
44
southeastern
Xing’an-Mongolia
40
Orogenic
Belt.
Two
samples
of
the
Ar-39Ar ages of 408 Ma from the overlying
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Introduction
46
Orogenic belts feature intense tectonic activities and have long been studied by
47
geologists. The Central Asian Orogenic Belt (CAOB) is one of the largest and
48
longest-lived Phanerozoic accretionary orogens on Earth, and it has experienced
49
multiple complex subduction-collision phases with various structural domains since the
50
late Mesoproterozoic (Fig. 1a, Tang 1990; Shao 1991; Sengör and Natal'in 1996; Khain
51
et al. 2002; Xiao et al. 2003, 2009; Jahn et al. 2004, Jian et al. 2008; Windley et al. 2007;
52
Zhang et al. 2014; Wang et al. 2015a). The Xing’an-Mongolia Orogenic Belt (XMOB,
53
i.e., the eastern section of the CAOB) is sandwiched between the Siberian Craton (SC)
54
in the north and the North China Craton (NCC) in the south (Fig. 1a). The tectonic
55
evolution of northeast (NE) China and adjacent regions located within the eastern
56
section of the XMOB was dominated by the assembly of several microcontinental
57
blocks (Fig. 1b) and the closure of the Palaeo-Asian ocean during the Palaeozoic to
58
early Mesozoic (JBGMR 1988; Li et al. 1999, 2006, 2014; Xu et al. 2003; Wu et al.
59
2007; Meng et al. 2010; Cao et al. 2013), with subsequent superimposition of the
60
Circum-Pacific and Mongolia Okhotsk tectonic systems during the Mesozoic (Ying et
61
al. 2008; Yu et al. 2012; Sun et al. 2013a; Tang et al. 2014).
62
The Yanbian area in eastern Jilin Province is located at the junction of NE China, Far
63
East Russia and Korea. Tectonically, it is located in the southeastern section of the
64
XMOB at the junction of the Khanka-Jiamusi block, the Songnen-Zhangguangcai
65
Range (SZR) massif and the NCC (Fig. 1b; Jia et al. 2004). The Yanbian area is
66
characterized by large volumes of Phanerozoic granitoids with small amounts of
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Palaeozoic to Mesozoic strata (Fang 1992; JBGMR 1988; Sun et al. 2013b) and the
68
existence of three types of flora (Cathaysian flora, Angara flora, mixed
69
Cathaysian-Angara flora; Peng et al. 1999). The strata are distributed among the
70
Phanerozoic granitoids in the forms of isolated islands, tectonic remnants and variously
71
sized xenoliths. The early Palaeozoic tectonic evolution of this area remains
72
controversial. Based on the analysis of pre-Mesozoic metamorphic rocks in the
73
Yanbian area, Wang (1998) proposed that the strata were deposited on deformed middle
74
and upper Proterozoic crust that was then deformed in an orogenic belt during the early
75
Palaeozoic. However, according to comparison of stratigraphic, petrological and
76
palaeontological data, Jia (1995) and Tang and Zhao (2007) suggested that the Yanbian
77
area, which differs from the surrounding massifs, is an allochthonous terrane.
78
Furthermore, there are two contrasting viewpoints on the tectonic setting of the Yanbian
79
area: passive continental margin (Jia et al. 2004) or active continental margin (Zhao et
80
al. 1996; Wang et al. 1997; Wang 1998).
81
These different interpretations arise from the paucity of reliable geochronologic and
82
geochemical data from the Palaeozoic strata in the Yanbian region. In this paper, we
83
present results from zircon U-Pb dating and Hf isotopic analyses as well as whole-rock
84
geochemical analyses of meta-sedimentary rocks in the Jiangyu Group at Kaishantun
85
town in the southern Yanbian region. These new results offer new evidence to better
86
understand the tectonic evolution of the southeastern section of the XMOB.
87
Geologic setting and sample descriptions
88
The Yanbian area is situated in the southeastern section of the CAOB and is
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sandwiched by the NCC, SZR massif and Khanka-Jiamusi block. These terranes are
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separated by the Gudonghe-Fuerhe-Chongjin fault belt (GFC), the Dunhua-Mishan
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fault belt (DM) and the Wangqing-Hunchun (WH) or Dashanzui-Antu-Kaishantun
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suture belt (DAK) , respectively (Fig. 1b; Zhao et al. 1996; Jia et al. 2004; Sun et al.
93
2013b). The Yanbian area was influenced by collisions between microcontinental
94
blocks and the NCC in the Palaeo-Asian ocean tectonic domain from the Paleozoic to
95
Early Triassic. Subsequently, the region was dominated by tectonic overprinting and
96
transformation related to the Circum-Pacific structural domain (Jia et al. 2004; Zhang et
97
al. 2004; Xu et al. 2013). Large volumes of Phanerozoic granitoids are widespread in
98
this area; however, Palaeozoic and Mesozoic rocks are rare and present as remnants in a
99
“sea” of granitoids (JBGMR 1988). The main Palaeozoic stratigraphic units in the
100
Yanbian area are distributed to the southwest of Kaishantun town in the southern
101
Yanbian area and are surrounded by intrusive Mesozoic granitoids. The strata in this
102
area are dominated by widespread upper Palaeozoic units, including the upper
103
Carboniferous Shanxiuling Formation, the Carboniferous to Permian Dasuangou
104
Formation and Hesheng Formation, and the lower Permian Miaoling Formation, as
105
well as Mesozoic and Cenozoic strata. The study area also features widespread
106
Mesozoic granitoids, as well as minor ophiolitic mélange and upper Permian
107
mafic-ultramafic rocks (Fig. 2; JBGMR 1988, 2000; Tang and Zhao 2007). Outcrops
108
are rare, and the terrane in this area is heavily forested. The Jiangyu Group is distributed
109
in the west of Jiangyu village to the southwest of Kaishantun town and mainly consists
110
of chlorite schist, biotite-plagioclase gneiss, two-mica schist, and magnetite quartzite.
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The samples used in this paper were collected from the Jiangyu Group.
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Sample HC-1 is a biotite-plagioclase gneiss from the Jiangyu Group that was
113
collected ~18 km to the southwest of Kaishantun town (GPS location: 42º32'51" N,
114
129º42'1" E; Fig. 2), to the south of Yanji City. In addition, we collected seven samples
115
(HC-2, 3, 4, 5, 6, 7 and 8) at the same location for whole-rock geochemical analysis
116
(Table S2). These charcoal grey rocks feature a medium- to fine-grained
117
lepidogranoblastic texture, gneissic structure and little sericitization. The samples are
118
composed of plagioclase (~40%), quartz (~39%), biotite (~16%), and muscovite (~5%),
119
with minor opaque minerals (Fig. 3a, b and c). Quartz aggregates exhibit a directional
120
strip-shaped arrangement. Biotite and muscovite display a continuous directional
121
arrangement, and the grains are bent. The plagioclase grains exhibit sericitization, and
122
the sericite is thin and flaky. Thus, the samples are mid-grade metamorphic products.
123
Sample HC-9 is a two-mica schist from the Jiangyu Group that was collected ~0.9
124
km to the southwest of HC-1 (GPS location: 42º32'50" N, 129º41'47" E; Fig. 2). In
125
addition, we also collected seven samples (HC-10, 11, 12, 13, 14, 15 and 16) from the
126
same location for whole-rock geochemical analysis (Table S2). The samples are grey
127
and characterized by a medium- to fine-grained lepidogranoblastic texture, weak
128
schistosity and sericitization (Fig. 3d, e and f). The samples contain quartz (~42%),
129
muscovite (~22%), plagioclase (~18%), biotite (~16%) and garnet (~2%), with minor
130
opaque minerals. Quartz aggregates exhibit a directional strip-shaped arrangement, and
131
the plagioclase grains display strong sericitization. Moreover, a small amount of
132
plagioclase is completely metasomatised, and the granular crystals of the original
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minerals are preserved. Biotite displays a flaky texture and continuous directional
134
arrangement. Additionally, some biotite was partially transformed into muscovite.
135
Sericite exhibits a thin and flaky composition. The garnet grains are cracked and
136
distributed in star shapes. Thus, the samples are mid-grade metamorphic products.
137
Methods
138
Zircon U-Pb dating
139
The samples were first crushed to 80-100 mesh, and the low-density minerals were
140
then removed using conventional heavy-liquid techniques. High-purity zircon samples
141
were then separated from the remaining heavy minerals using magnetic separation
142
techniques at the Langfang Regional Geological Survey, Hebei Province, China.
143
High-quality non-fractured zircon grains were inlaid in epoxy, polished down to half
144
their original thickness and washed in an acid bath before analysis. Transmitted light
145
and reflected light images were captured using a microscope, and cathodoluminescence
146
(CL) images were collected using a JEOL scanning electron microscope at the State
147
Key Laboratory of Continental Dynamics, Northwest University, Xi’an, China. Based
148
on analysis of the CL images, distinct locations within the zircons were selected as the
149
best points for laser ablation inductively coupled plasma mass spectrometer
150
(LA-ICP-MS) measurements. An Agilent 7500a ICP-MS equipped with ComPex 102
151
ArF excimer laser was used to measure the U-Pb isotope ages of the zircons. Helium
152
gas was used as the carrier gas, and a crater diameter of 30 µm and a laser intensity of
153
50 J cm-1 were used in all analyses. The standard zircon 91500 was used as the external
154
age calibration standard. In addition, the standard material NIST 610 was used as the
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external standard to calculate the trace element concentrations in the zircons, and 29Si
156
was used as an internal standard to calibrate the contents of U, Th and Pb in the zircons.
157
The detailed instrument operating conditions and data processing methods were
158
described by Yuan et al. (2004). Common Pb corrections were performed using the
159
method of Anderson (2002). The isotope ratio and element content calculations for
160
zircon dating were performed using GLITTER (ver. 4.0), and the age calculations and
161
concordia diagrams were generated using Isoplot (Ludwig, 2003). Individual analyses
162
of the isotope ratio and age error (standard error) are reported at the 1 sigma level, and
163
errors in the weighted mean
164
confidence level.
165
Major and trace element analyses
207
Pb/206Pb ages are reported at the 95% (2 sigma)
166
After removal of altered surfaces, whole-rock samples were crushed to ~200 mesh.
167
The whole-rock major and trace element compositions of the samples were determined
168
at the Supervision and Inspection Center of Mineral Resources, the Ministry of Land
169
and Resources of Jinan, China. The contents of SiO2 and Al2O3 were analysed via the
170
gravimetric approach based on gelatin coagulation and the xylenol orange method,
171
respectively. The concentrations of major oxides (Fe2O3, CaO, MgO, FeO, K2O, Na2O,
172
TiO2, MnO, and P2O5) and trace elements, including Ba, Sr, V, and Cr, were measured
173
using an IRI-Intrepid plasma spectrometer and the standard GB/T14506-2010 for the
174
oxides. The remaining trace elements were determined using an XSeries 2 ICP-MS.
175
Zircon Hf isotopic analyses
176
Zircon Hf isotope analyses were performed at the State Key Laboratory of
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Continental Dynamics, Northwest University, China, using a Nu Plasma HR
178
multicollector (MC) ICP-MS coupled with a Geolas 200M laser ablation system made
179
by the German Microlas company. The Hf analyses were performed on the same spots
180
as the previous U-Pb isotope analyses, with a spot size of 44 µm and a repetition rate of
181
10 Hz. Detailed instrument operating conditions and data processing methods were
182
described by Yuan et al. (2008). Isobaric interference corrections for the sample
183
176
Lu/177Hf and
184
176
Lu/175Lu=0.02669 (Biévre and Taylor 1993) and
185
2002). During the analyses, instrument monitoring and sample correction were
186
performed using the zircon standards 91500 and GJ-1. The
187
standard 91500 is 0.282295±0.000029 (n=17, 2σ), which is relatively consistent with
188
the recommended value (0.2823075±0.000058, 2σ, Wu et al. 2006). The
189
constant of 1.867×10-11 year-1 (Albarède et al. 2006) and the present-day chondritic
190
ratios of 176Hf/177Hf = 0.282785 and 176Lu/177Hf = 0.0336 were adopted to calculate the
191
ƐHf(t) values (Bouvier et al. 2006). Single-stage model ages (TDM1) were calculated
192
based on a depleted mantle with a present-day
193
176
194
calculated using an assumed 176Lu/177Hf ratio of 0.01544 for average continental crust
195
(Rudnick and Gao, 2003).
196
Results
197
Zircon U-Pb dating
198
176
Hf/177Hf ratios were applied based on the values of 176
Yb/172Yb=0.5886 (Chu et al.
176
Hf/177Hf ratio of zircon
176
Lu decay
176
Hf/177Hf ratio of 0.28325 and an
Lu/177Hf ratio of 0.0384 (Vervoort et al. 1999). Two-stage model ages (TDM2) were
Most zircon grains from sample HC-1 are euhedral to subhedral in the CL images,
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and some display oscillatory zoned cores with homogeneous rims that are too narrow to
200
be analyzed, suggesting that these grains may have experienced a late metamorphic
201
event (Fig. 4a; Wang et al 2014). The Th/U ratios are between 0.11 and 1.28 (excluding
202
one analysis, HC-1-76, with a Th/U ratio of 0.03), indicating a magmatic origin
203
(Koschek 1993). Some zircon grains are rounded to subrounded, and some contain
204
inherited core-rim textures in the CL images (Fig. 4a). A total of one hundred and one
205
analyses were performed on one hundred grains, and the results are presented in Table
206
S1. Apart from seven analyses (HC-1-01, 42, 59, 79, 88, 90 and 99), the other
207
ninety-four U-Pb analyses were less than 10% discordant and yielded ages of 418±6 to
208
2658±12 Ma (Fig. 5a) that can be divided into three age populations: a main age
209
population of 418-494 Ma (n=61, with one peak value at 454 Ma and two weak peaks at
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428 and 473 Ma; Fig. 5b, c) and two secondary age populations of 562-657 Ma (n=10,
211
with peak values at 569 and 633 Ma) and 889-1259 Ma (n=13, with peak values at 933
212
and 1091 Ma, respectively). Additionally, other individual ages and minor groups
213
include 1442, 1587-1616, 1770-1832, 1979, 2288, 2439 and 2658 Ma (n=10; Fig. 5a, c).
214
Notably, one grain from the sample HC-1 with a core-rim texture yielded a core age of
215
2591±14 Ma (HC-1-42) and a rim age of 562±6 Ma (HC-1-43) (Fig. 4a).
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The majority of grains from sample HC-9 are euhedral to subhedral in the CL
217
images and exhibit oscillatory growth zoning and internal core-rim structures (Fig. 4b).
218
The Th/U ratios are between 0.12 and 1.54, suggesting a magmatic origin (Koschek
219
1993). Some zircons are rounded to subrounded, and some contain inherited core-rim
220
textures in the CL images (Fig. 4b). Additionally, some zircons in this sample have thin
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homogenous rims, suggesting they may have experienced a late metamorphic event
222
(Wang et al. 2014). Overall, ninety-six analyses were performed on ninety-six grains,
223
and the results are presented in Table S1. Apart from four analyses (HC-9-39, 79, 86
224
and 93), the other ninety-two U-Pb analyses were less than 10% discordant and yielded
225
ages of 415±9 Ma to 2926±28 Ma (Fig. 5d) that can be divided into four age
226
populations: a main age population of 415-504 Ma (n=52, with peak values at 428 Ma,
227
455 Ma and 478 Ma) and three secondary age populations of 567-649 (n=7, with a peak
228
value at 597 Ma), 933-1138 Ma (n=9, with peak values at 943 Ma and 1124 Ma) and
229
1607-1866 Ma (n=12, with peak values at 1676 Ma and 1800 Ma). In addition,
230
individual and minor group ages of 1225-1529, 2408-2462, 2597, 2636 and 2926 Ma
231
were also obtained (n=12; Fig. 5d, f).
232
Geochemistry
233
Major element compositions
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The metamorphic rocks of the Jiangyu Group have compositions of
235
SiO2=64.54-68.20
wt.%,
TiO2=0.63-0.79
236
Fe2O3T=5.78-7.07
wt.%,
237
K2O+Na2O=4.19-5.15 wt.%, and SiO2/Al2O3=4.20-4.88 (Table S2). The average major
238
element contents of the samples are highly consistent with normalized upper
239
continental crust (UCC) values, except for their low CaO, Na2O, and K2O contents
240
(Rudnick and Gao 2003). However, in comparison with post-Archean average shale
241
(PAAS), the samples have low Fe2O3T, TiO2, Al2O3, and K2O contents and high SiO2,
242
Na2O, CaO, and MgO contents (Table S2; McLennan et al. 1993).
Na2O=1.58-2.53
wt.%, wt.%,
Al2O3=13.65-15.35
wt.%,
K2O=2.00-3.16
wt.%,
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Trace element compositions
244
According to the chondrite-normalized rare earth element (REE) diagram (Fig. 6a;
245
Sun and McDonough 1989), these samples are enriched in light REEs (LREEs),
246
depleted in heavy REEs (HREEs), and feature ∑LREE/∑HREE ratios of 5.83-8.52.
247
Furthermore, the total REE abundances are low (∑REE=139-198 ppm, average=157
248
ppm). These patterns are generally similar to those of the UCC and PAAS, although the
249
sample patterns differ somewhat from the UCC patterns in terms of HREEs (Fig. 6a).
250
The REE patterns are moderately fractionated, with (La/Yb)N ratios that vary from 5.60
251
to 8.97 (average=6.92) and weakly negative Eu anomalies of 0.61-0.81 (average=0.69,
252
Fig. 6a; Table S2). On the UCC-normalized variation diagram, these rocks are depleted
253
in large ion lithophile elements (LILEs; e.g., Rb, Sr, and Ba) and enriched in high field
254
strength elements (HFSEs; e.g., Ta, Y, and U) and Pb (Fig. 6b; Rudnick and Gao 2003).
255
Furthermore, the LILE and HFSE contents of PAAS are mostly higher than those of the
256
studied samples; in contrast, the Dy, Er, Yb, and Lu contents of PAAS are lower than
257
those of the Jiangyu Group samples (Fig. 6b; Table S2). Additionally, the samples have
258
high Cr (247.6-382.7) and Co (13.03-20.25) concentrations.
259
Zircon Hf isotopes
260
Some of the zircon grains analysed for U-Pb dating were also analysed via in situ Hf
261
isotopic analysis. The results are shown in Fig. 7a-b and are listed in Supplementary
262
Table 3.
263
A total of 44 detrital zircons from sample HC-1 were chosen for Hf isotopic
264
composition analysis. One Archean (2658 Ma) zircon yielded a negative ƐHf(t) value of
Page 13 of 62
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-6.99 and TDM2 age of 3558 Ma. Three zircons with Palaeoproterozoic U-Pb ages (2439
266
to 1832 Ma) yielded negative ƐHf(t) values from -10.07 to -4.08 and TDM2 ages of
267
3358-2852 Ma; the remaining zircons yielded positive ƐHf(t) values between 1.90 to
268
9.84 and corresponding TDM2 ages of 2320-1869 Ma. Most of the Mesoproterozoic
269
detrital zircons yielded positive values of 0.61 to 9.92 and TDM2 ages of 2256-1315 Ma;
270
the remaining two Mesoproterozoic zircons yielded negative ƐHf(t) values of -3.60 and
271
-8.35 and corresponding TDM2 ages of 2403 and 2439 Ma, respectively. The
272
Neoproterozoic zircons yielded positive ƐHf(t) values ranging from 0.11 to 10.85 and
273
TDM2 ages of 1498-1093 Ma, barring one zircon (934 Ma) with a negative ƐHf(t) value
274
of -1.14 and a TDM2 age of 1853 Ma. The majority of detrital zircons in the 487-420 Ma
275
population yielded positive ƐHf(t) values from 2.39 to 13.56, with TDM2 ages of
276
1240-540 Ma; the remaining early Palaeozoic zircons in this group yielded negative
277
ƐHf(t) values from -7.29 to -0.05, with TDM2 ages of 1870-1393 Ma.
278
A total of 45 detrital zircons from sample HC-9 were chosen for Hf isotopic analysis.
279
Two Archean (2636 and 2597 Ma) zircon grains yielded positive ƐHf(t) values of 1.75
280
and 4.91, with TDM2 ages of 3012 and 2789 Ma, respectively. Most of the
281
Palaeoproterozoic zircon grains yielded positive ƐHf(t) values between 1.35 and 10.11,
282
with TDM2 ages of 2342-1870 Ma; the secondary Palaeoproterozoic zircon grain
283
population yielded negative ƐHf(t) values of -5.01 to -2.95, with corresponding TDM2
284
ages of 3134-2767 Ma. Detrital zircons with concordant ages of 1529 to 933 Ma
285
yielded positive ƐHf(t) values from 1.13 to 9.43 and TDM2 ages of 2178-1466 Ma,
286
barring one grain with a ƐHf(t) value of -0.13 and a TDM2 age of 1790 Ma. All detrital
Page 14 of 62
287
zircons with concordant ages of 649-567 Ma yielded positive ƐHf(t) values between
288
1.71 and 6.70 and TDM2 ages of 1452-1072 Ma. The majority of the detrital zircons in
289
the 504-415 Ma age population yielded positive ƐHf(t) values of 0.67 to 10.57, with
290
TDM2 ages of 1378-735 Ma; the remaining Phanerozoic detrital grains yielded negative
291
ƐHf(t) values from -18.95 to -3.55 and TDM2 ages of 2613-1656 Ma.
292
Discussion
293
Protolith reconstruction
294
The study area experienced intensive erosion and various degrees of deformation
295
and metamorphism during late tectonic and/or magmatic events (Jia et al. 2004).
296
Consequently, fluid-mobile elements in the rocks may have experienced various
297
degrees of reallocation during metamorphism. However, considerable information
298
related to the nature of the protoliths and tectonic setting can be obtained from the
299
concentrations and ratios of these relatively immobile elements relative to those of
300
fluid-mobile elements (Shaw 1972; Bhatia 1983; Bhatia and Crook 1986). Hence, we
301
primarily use immobile elements to determine the nature of the protoliths and tectonic
302
setting using other elements as a reference.
303
The discriminant function (DF) (Shaw 1972), TiO2-SiO2 diagram (Tarrey et al.
304
1976), Niggli parameter diagram (Simonen 1953), and log(Na2O/K2O)-log(SiO2/Al2O3)
305
diagram (Pettijohn et al. 1987) methods were used to reconstruct the protoliths. All DF
306
values for the studied samples were negative (ranging from -3.83 to -2.13), indicating
307
probable sedimentary parentage. This conclusion is supported by the TiO2-SiO2
308
discrimination diagram (Fig. 8a). In the Niggli parameter discrimination diagram, the
Page 15 of 62
309
samples plot in the sedimentary rock domain (Fig. 8b), suggesting that these samples
310
are sedimentary in origin. The log(Na2O/K2O)-log(SiO2/Al2O3) diagram developed by
311
Pettijohn et al. (1987) demonstrates that these samples were derived from graywacke
312
(Fig. 8c).
313
The depositional age of the Jiangyu Group
314
Since it is hard to directly obtain the ages of rocks based on the lithostratigraphic
315
or biostratigraphic relationships with other strata in this region, the protolith
316
depositional age of the Jingyu Group cannot be corroborated by other datasets. Notably,
317
the
318
Permo-Carboniferous in age (JBGMR 1988, 2000; Tang and Zhao 2007). It is generally
319
accepted that the maximum age of deposition may be older than the actual time of
320
sedimentary deposition based on the ages of the youngest zircon or zircons (Nelson
321
2001; Fedo 2003; Dickinson and Gehrels 2009; Gehrels 2014). The reliable youngest
322
age approach is based on the youngest concordant zircon U-Pb age, the youngest peak
323
age or the mean age of the youngest zircons (n≥2) with ages overlapping at 1 sigma
324
(YC1σ(2+)) (Dickinson and Gehrels 2009). Here, we opt to use the YC1σ(2+) approach
325
as a reliable estimate of the maximum depositional age of the Jiangyu Group to reduce
326
the impact of later tectonothermal events and the uncertainty related to the analysis of
327
detrital zircons. Our new zircon U-Pb dating results for the detrital grains from HC-1
328
show that the youngest zircon population (ca. 438-418 Ma) yields a weighted mean age
329
of 426±3 Ma (MSWD=1.10, n=18; Fig. 5b), suggesting that the protolith of the
330
biotite-plagioclase gneiss was not deposited prior to 426 Ma. Furthermore, concordant
group
has
previously
been
considered
Precambrian,
Cambrian
or
Page 16 of 62
331
detrital grains from sample HC-9 produced results that are essentially in agreement
332
with HC-1. The youngest zircon population (ca. 436-415 Ma) from sample HC-9 yields
333
a weighted mean age of 427±3 Ma (MSWD=0.91, n=15; Fig. 5e), suggesting that the
334
protolith of the two-mica schist was deposited after ca. 427 Ma. Consequently, the
335
detrital zircon results show that the protoliths of the Jingyu Group were deposited no
336
earlier than the late Silurian. Based on the published reliable muscovite 40Ar-39Ar age of
337
408 Ma from the overlying metamorphic ophiolitic mélange (Tang and Zhao 2007), the
338
Jiangyu Group likely formed before 408 Ma. We conclude, therefore, that the protoliths
339
of the group were deposited during the late Silurian-early Devonian and not during the
340
Precambrian, Cambrian or Permo-Carboniferous, as previously claimed.
341
Sedimentary provenance of the Jiangyu Group and its tectonic affinity
342
Zircon is characterized by its high weathering resistance and a high U-Pb closure
343
temperature; thus, zircon grains feature a U-Pb isotopic system that remains stable
344
throughout various geological processes (Bruguier et al. 1997; Cherniak and Watson
345
2000). Therefore, it is generally accepted that the age spectra of detrital zircons from
346
sedimentary rocks can retain information regarding the depositional provenance and
347
can be used to reconstruct the tectonic evolution of ancient basins and orogenic belts
348
(Carter and Steve 1999; Fedo et al. 2003; Rojas-Agramonte et al. 2011; Wang et al.
349
2016).
350
In total, 186 of the 197 analyses of the two samples yield concordant ages (less than
351
±10% discordant) ranging from 2926 Ma to 415 Ma, with prominent age peaks at 428,
352
455, 476, 564, 622, 935, 1124, 1676 and 1816 Ma and minor peaks at 889, 1529-1313,
Page 17 of 62
353
1979, 2288, 2649-2423 and 2926 Ma (Fig. 9d).
354
In the Jiangyu Group, most detrital zircons produced concordant ages ranging
355
from 504 to 415 Ma, with peaks at 476, 455 and 428 Ma. These data are comparable
356
with the ages of lower Palaeozoic igneous rocks in the SZR massif, the Jiamusi massif
357
(Liu et al. 2008; Wang et al. 2012a), central Jilin Province (Pei et al. 2015) and central
358
Inner Mongolia (Jian et al. 2008; Guo et al. 2009; Zhang et al. 2014). Additionally,
359
these data are concordant with the early Palaeozoic detrital zircon ages reported from
360
the lower Permian Hesheng Formation (Sun et al. 2013b) and the upper Permian
361
Dasuangou and Miaoling formations (Zhou et al. 2017) in this area. Furthermore,
362
similar detrital zircon or inherited zircon ages are common in the sedimentary and
363
igneous rocks in other parts of the eastern margin of the XMOB (Wilde et al. 2003;
364
Gladkochub 2008; Meng et al. 2010; Zhou et al. 2010a; Wang et al. 2012a, 2012b, 2014,
365
2015b; Pei et al. 2015). Moreover, the Hf isotopic compositions (ƐHf(t) values of -3.55
366
to 13.56, with TDM2 ages of 1656 to 540 Ma) of the majority of early Palaeozoic detrital
367
zircons are analogous to those of coeval grains from the eastern XMOB (Guo et al.
368
2009; Wang et al. 2012b, 2015a; Pei et al. 2014;2015), suggesting that these detrital
369
zircons may have originated from juvenile crust within the eastern XMOB. Therefore,
370
the early Palaeozoic detrital zircons of the Jiangyu Group may have been
371
predominantly sourced from the eastern XMOB.
372
In the Jiangyu Group, detrital grains with ages of 562-657 Ma and 889-1268 Ma
373
reveal that the provenance of these rocks included considerable proportions of upper
374
Mesoproterozoic and Neoproterozoic magmatic rocks. Zircons with ages of 562-657
Page 18 of 62
375
Ma are rare in the metamorphic rocks of the eastern XMOB (Fig. 9a; Wilde et al. 2000,
376
2003; Zhou et al. 2010a, 2010b). However, the detrital or inherited zircon age group of
377
ca. 800 Ma, which is common in the Palaeozoic terranes and older rock groups in the
378
microcontinents of the eastern XMOB (Fig. 9a; Stern 2008; Zhou et al. 2012; Wang et
379
al. 2014), is absent in the Jiangyu Group, and late Mesoproterozoic magmatism
380
(1268-1000 Ma) has not been reported in the eastern XMOB (Meng et al. 2010; Li et al.
381
2011a; Wu et al. 2011; Wang et al. 2014). The NCC also does not record evidence of
382
late Meso-Neoproterozoic magmatism (Fig. 9b; Cope et al. 2005; Li et al. 2009; Zhao
383
and Guo, 2012b). Therefore, these microcontinents and the NCC are not considered
384
potential source areas for the late Meso-Neoproterozoic detrital zircons of the Jiangyu
385
Group. However, detrital zircon populations from ca. 650-550 Ma and ca. 1200-900 Ma
386
accounted for high proportions of the lower to middle Cambrian clastic strata in
387
terranes located along the northeastern margin of Gondwana during the early
388
Palaeozoic (Fig. 9c; Li et al. 2001; Squire et al. 2006; Wang et al. 2016), e.g., Australia
389
(Ireland and Bowring 1998), Antarctica (Goodge et al. 2004), New Zealand (Richard
390
Jongens et al. 2003), and northern India (Myrow et al. 2003). These late
391
Meso-Neoproterozoic detrital grains from the Jiangyu Group are primarily euhedral to
392
subhedral, indicating that they likely experienced only short-distance transport in the
393
sedimentary regime. Therefore, these zircons were potentially derived from a local
394
source, suggesting that a Precambrian crystalline basement may have existed in the
395
southern Yanbian region and may have supplied material to the Jiangyu Group. In
396
addition, these late Meso-Neoproterozoic detrital zircons yield ƐHf(t) values ranging
Page 19 of 62
397
from -8.35 to +10.85 and TDM2 ages of 2439 to 1093 Ma and consequently resemble
398
zircons from northeastern Gondwana (Fig. 7a, b; Kemp et al. 2006; Ravikant et al. 2011;
399
Wang et al. 2016). Furthermore, the fossil assemblages of the upper Carboniferous
400
Shanxiuling Formation and lower Permian Miaoling Formation in this area resemble
401
those of the Gondwanan and Tethyan tectonic domains but not those from the adjacent
402
domains (Jia 1995). Therefore, we suggest that the late Meso-Neoproterozoic detrital
403
zircons of the Jiangyu Group were likely sourced from a ‘missing’ local Precambrian
404
basement with a tectonic affinity to northeastern Gondwana.
405
In the Jiangyu Group, the detrital zircons with ages of 1607-1979 Ma and
406
2288-2926 Ma reveal that Mesoarchaean and Palaeoproterozoic magmatic rocks were a
407
source of sediment. These two groups, which are related to magmatic-thermal events,
408
are widespread in the SC, Tarim Craton (TC), and NCC (Zhai et al. 2005; Rosen et al.
409
2006; Sal’nikova et al. 2007; Lu et al. 2008; Li et al. 2009; Long et al. 2010; Meng et al.
410
2010; Zhu et al. 2011; Zhao et al. 2012a; Liu et al. 2013) and are also present in the
411
form of detrital zircons or inherited or magmatic zircons within magmatic rocks in
412
Palaeozoic metamorphic complexes and strata in NE China (Miao et al. 2007; Pei et al.
413
2007; Chen et al. 2009; Li et al. 2005; 2010). Additionally, zircons of similar age were
414
observed as igneous and detrital zircons in regions that formerly comprised
415
northeastern Gondwana (Condie et al. 2009; Rojas-Agramonte et al. 2011). However,
416
despite the similarity of the age associations (~2500 Ma and ~1800 Ma) to those in the
417
TC and SC, we suggest that these ancient zircon-bearing sediments of the Jiangyu
418
Group were most likely not sourced from these cratons based on the location of the
Page 20 of 62
419
study area in the southeastern XMOB and far from these cratons (Fig. 1a). In addition,
420
these Palaeoproterozoic and Archean detrital zircons are predominantly euhedral to
421
subhedral (Fig. 4a, b), indicating that they experienced relatively minimal transport
422
prior to deposition. Therefore, these zircons might have been sourced from the missing
423
local Precambrian basement with a tectonic affinity to northeastern Gondwana or the
424
eastern XMOB. In contrast, the remaining zircons are rounded to subrounded,
425
indicating that they experienced long-distance transport before deposition. This
426
observation suggests that these zircons might have been sourced from the NCC.
427
In conclusion, the Palaeozoic detrital zircons of the Jiangyu Group were sourced
428
predominantly from the eastern XMOB. The Meso-Neoproterozoic detrital grains of
429
the group were like sourced from a missing local Precambrian basement with a tectonic
430
affinity to northeastern Gondwana. Similarly, the Palaeoproterozoic and Archean
431
detrital grains of the group were potentially sourced from the same missing local
432
Precambrian basement or from the eastern XMOB and to a lesser degree from the NCC.
433
Depositional setting
434
The protoliths of meta-sedimentary rocks in different tectonic environments have
435
different geochemical characteristics, and these characteristics can be used to determine
436
the sedimentary tectonic setting (Bhatia 1983). Based on the tectonic setting
437
discrimination diagrams for clastic rocks proposed by Roser and Korsch (1986), the
438
tectonic setting can be divided into passive continental margin (PM), active continental
439
margin (ACM) and oceanic island arc (OIA). In the K2O/Na2O-SiO2 discrimination
440
diagram (Fig. 10a), all the samples from the Jiangyu Group plot in the ACM domain.
Page 21 of 62
441
Similarly, these results are supported by the SiO2/Al2O3-K2O/Na2O tectonic diagram
442
(Fig. 10b; Maynard et al. 1982).
443
Furthermore, Bhatia and Crook (1986) demonstrated that immobile trace elements
444
in meta-sedimentary rocks can be used to discriminate among various tectonic settings.
445
In the La-Th-Sc diagram (Fig. 11a), all samples from the Jiangyu Group plot in the
446
continental island arc (CIA) domain. Moreover, the same results are obtained from the
447
Th-Sc-Zr/10 and Ti/Zr-La/Sc discrimination diagrams (Fig. 11b, c). An ‘island’ arc is
448
typically defined as a magmatic arc that has formed in the ocean, forming islands, via
449
oceanic-oceanic subduction; however, an arc that has formed in continental crust via
450
the subduction of oceanic crust beneath a continent is in nature a continental arc,
451
regardless of whether it has been rifted away from the continent via back-arc extension.
452
In this study, all the samples from the Jiangyu Group exhibit typical continental arc
453
geochemical signatures instead of island arc signatures. Therefore, the protolith of
454
these meta-sedimentary rocks was deposited in a continental arc setting. These results
455
are supported by the comparison of the average REE values from the Jiangyu Group
456
samples and those from various tectonic settings (Table 1; Bhatia 1985). The
457
remarkable similarities in the average REE values between the Jiangyu Group samples
458
and the CIA setting suggest that the protoliths of the Jiangyu Group were deposited in a
459
continental arc setting.
460
In summary, the characteristics of the meta-sedimentary Jiangyu Group are
461
consistent, in terms of both major elements and trace elements, with rocks formed in a
462
continental arc tectonic setting related to an ACM. Based on these data and the results
Page 22 of 62
463
of the sedimentary provenance analysis, the Jiangyu Group may represent a continental
464
arc terrane with a tectonic affinity to northeastern Gondwana.
465
Tectonic implications
466
The results presented here indicate that an upper Silurian-Lower Devonian terrane is
467
present in the southern Yanbian area. The precise geochronological data from detrital
468
zircons from the Jiangyu Group have constrained the sedimentary provenance of the
469
meta-sedimentary rocks and have provided us with a new understanding of the
470
Palaeozoic tectonic evolution of the southeastern section of the XMOB.
471
Based on the comparisons of the detrital zircon U-Pb ages and Hf isotopic data
472
between northeastern Gondwana and the Jiangyu Group (Fig. 9a, b; Kemp et al. 2006;
473
Ravikant et al. 2011; Wang et al. 2016), we propose that the Jiangyu continental arc
474
terrane is an allochthon that originated in northeastern Gondwana, similar to the
475
Khanka-Jiamusi block (Wilde et al. 2000; Yang et al. 2014). This hypothesis is
476
supported by the findings of Jia (1995) based on comparisons of palaeomagnetic data
477
and fossil assemblages between the upper Carboniferous Shanxiuling Formation and
478
lower Permian Miaoling Formation in the Yanbian region and adjacent areas.
479
Unfortunately, due to the absence of accurate palaeomagnetic data for the Jiangyu
480
continental arc terrane, the exact location of the Jiangyu block with respect to
481
northeastern Gondwana is difficult to determine. However, based on the existence of
482
the detrital zircon ages of 562-657 Ma (with peaks at 564 and 622; Fig. 9d) and
483
palaeogeographic reconstructions (Li et al. 2001), we suggest that the Jiangyu
484
continental arc terrane rifted from the margin of northeastern Gondwana after 564 Ma
Page 23 of 62
485
and drifted to the northern NCC (Fig.12). Additionally, age information on the late
486
Pan-African events is widely recorded in the eastern XMOB, as supported by previous
487
research (Wilde et al. 2000, 2010; Zhou et al. 2010b, 2011, 2012; Yang et al. 2014;
488
2017). However, evidence of Pan-African events is not present in the Jiangyu Group,
489
indicating that the Jiangyu continental arc terrane may have been part of the
490
structural fabric of the southeastern section of the XMOB since the Early Ordovician
491
(at approximately 476 Ma; Fig.12).
492
Previous studies have shown that an accretion zone related to multiple arc-continent
493
collisions existed along the eastern segment of the northern margin of the NCC in the
494
Early to Middle Paleozoic (Fig.13; Jiang et al. 2014; Zhang et al. 2014; Pei et al. 2015;
495
Wang et al. 2016; Han et al. 2018). This subduction-accretion process may have
496
extended eastward to the Yanbian area and continued through the Early Devonian based
497
on the continental arc depositional setting of the meta-sedimentary rocks in the upper
498
Silurian-Lower Devonian Jiangyu Group. Therefore, based on the presence of
499
meta-ophiolites with two different ages within the upper Carboniferous Shanxiuling
500
Formation overlying the Jiangyu Group (Shao and Tang 1995), an early Palaeozoic
501
accretion zone may have existed in the Yanbian area, and an arc-continent collision
502
may have occurred after the Early Devonian.
503
Conclusions
504
1. The protoliths of the Jiangyu Group meta-sedimentary rocks were deposited
505
during the late Silurian-early Devonian and not during the Precambrian, Cambrian or
506
Permo-Carboniferous, as previously suggested. Additionally, the protoliths of the
Page 24 of 62
507
meta-sedimentary rocks from the Jiangyu Group were graywackes.
508
2. The U-Pb and Hf isotopic results for detrital zircons from the Jiagyu Group
509
suggest that the protolith sediments of the meta-sedimentary units were mainly sourced
510
from juvenile crust in the eastern XMOB, with minor ancient clastic material possibly
511
derived from Precambrian rocks with a tectonic affinity to northeastern Gondwana, the
512
NCC or the eastern XMOB.
513
3. The Jiangyu terrane is an allochthon that originated in northeastern Gondwana,
514
and it has participated in the tectonic evolution of the eastern XMOB since the Early
515
Ordovician (approximately 476 Ma).
516
4. The meta-sedimentary rocks of the upper Silurian-Lower Devonian Jiangyu
517
Group were deposited in a continental arc setting. An early Palaeozoic accretion zone
518
may have existed in the Yanbian area and may have continued until the Early Devonian,
519
and an arc-continent collision may have occurred after the Early Devonian.
520 521
Acknowledgements
522
We thank the staff of the State Key Laboratory of Continental Dynamics, Northwest
523
University, Xi’an, China, for their advice and assistance during the zircon U-Pb and Hf
524
isotopic analyses. We appreciate the Supervision and Inspection Center of Mineral
525
Resources, the Ministry of Land and Resources of Jinan, China, for their assistance
526
with the major and trace element analysis. This work was financially supported by the
527
National Natural Science Foundation of China (grant no. 41372108 and 41602110),
528
Taishan Scholar Talent Team Support Plan for Advanced & Unique Discipline Areas),
Page 25 of 62
529
Major Scientific and Technological Innovation Projects of Shandong Province (grants
530
no. 2017CXGC1602 and 2017CXGC1603) and the SDUST Research Fund (grant no.
531
2015TDJH101).
532 533
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908
the Jiamusi-Khanka Block, NE China: Petrogenesis and geodynamic implica-
909
tions. Lithos, 208-209: 220-236. doi:10.1016/j.lithos.2014.09.019.
910
Yang, H., Ge, W.C., Zhao, G.C., Bi, J.H., Wang, Z.H., Dong, Y., and Xu, W.L. 2017
911
Zircon U-Pb ages and geochemistry of newly discovered Neoproterozoic orthogn-
912
eisses in the Mishan region, NE China: Constraints on the high-grade metamorph-
913
ism and tectonic affinity of the Jiamusi-Khanka Block. Lithos, s 268-271: 16-31.
914
doi: 10.1016/j.lithos.2016.10.017.
915
Ying, J.F., Zhou, X.H., Zhang, L.C., Wang, F., and Zhang, Y.T. 2008. Geochronologic-
916
al and geochemical investigation of the late mesozoic volcanic rocks from the
917
northern great xing’an range and their tectonic implications. International Journal
918
of Earth Sciences, 99: 357-378.
919
Yuan, H., Gao, S., Liu, X., Li, H., Günther, D., and Wu, F. 2004. Accurate U-Pb age and
920
trace element determinations of zircon by laser ablation-inductively coupled
921
plasma-mass spectrometry. Geostandards and Geoanalytical Research, 28: 353-
922
370. doi:10.1111/j.1751-908X.2004.tb00755.x.
923
Yuan, H.L., Gao, S., Dai, M.N., Zong, C.L., Günther, D., Fontaine, G.H., Liu, X.M., and
924
Diwu, C.R. 2008. Simultaneous determinations of U-Pb age, Hf isotopes and trace
Page 43 of 62
925
element compositions of zircon by excimer laser-ablation quadrupole and
926
multiple-collector ICP-MS. Chemical Geology, 247: 100-118. doi:10.1016/j.che-
927
mgeo.2007.10.003.
928
Yu, J.J., Wang, F., Xu, W.L., Gao, F.H., and Pei, F.P. 2012. Early Jurassic mafic
929
magmatism in the Lesser Xing'an-Zhangguangcai Range, NE China, and its
930
tectonic implications: Constraints from zircon U-Pb chronology and geochemistry.
931
Lithos, 142-143: 256-266. doi:10.1016/j.lithos.2012.03.016.
932
Zhai, M., Guo, J., and Liu, W. 2005. Neoarchean to Paleoproterozoic continental
933
evolution and tectonic history of the North China Craton: a review. Journal of Asian
934
Earth Sciences, 24: 547-561. doi:10.1016/j.jseaes.2004.01.018.
935
Zhang, Y.B., Wu, F.Y., Wilde, S.A., Zhai, M., Lu, X., and Sun, D. 2004. Zircon U-Pb
936
ages and tectonic implications of ‘Early Paleozoic’ granitoids at Yanbian, Jilin
937
Province, northeast China. Island Arc, 13: 484-505. doi:10.1111/j.1440-1738.2004.
938
00442.x.
939
Zhang, S.H., Zhao, Y., Ye, H., Liu, J.M., and Hu, Z.C. 2014. Origin and evolution of the
940
bainaimiao arc belt: implications for crustal growth in the southern Central Asian
941
Orogenic Belt. Geological Society of America Bulletin, 126: 1275-1300.
942
doi:10.1130/B31042.1.
943
Zhao, C.J., Peng, Y.J., Dang, Z.X., and Zhang, Y.P. 1996. Tectonic Framework and
944
Crust Evolution of Eastern Jilin and Heilongjiang Provinces. Shenyang: Liaoning
945
University Press 186 pp (in Chinese with English abstracts).
946
Zhao, G.C, Cawood, P.A., Li, S., Wilde, S.A., Sun, M., Zhang, J., He, Y.H., and Yin,
Page 44 of 62
947
C.Q. 2012a. Amalgamation of the North China Craton: Key issues and discussion.
948
Precambrian Research, 222-223:55-76. doi: 10.1016/j.precamres.2012.09.016.
949
Zhao, G.C., and Guo, J.H. 2012b. Precambrian geology of China: preface. Precam-
950
brian Research, 222-223: 1-12. doi:10.1016/j.precamres.2012.09.018.
951
Zhou, J.B, Wilde, S.A., Zhao, GC. Zhang, X.Z., Wang, H., and Zeng, W.S. 2010a. Was
952
the easternmost segment of the Central Asian Orogenic Belt derived from
953
Gondwana or Siberia: An intriguing dilemma? Journal of Geodynamics, 50: 300-
954
317. doi:10.1016/j.jog.2010.02.004.
955
Zhou, J.B., Wilde, S. A., Zhao, G., Zhang, X., Zheng, C., and Zeng, H.W.W. 2010b.
956
Pan-african metamorphic and magmatic rocks of the Khanka massif, NE China:
957
further evidence regarding their affinity. Geological Magazine, 147: 737-749. doi:
958
10.1017/S0016756810000063.
959
Zhou, J.B., Wilde, S.A., Zhang, X.Z., Ren, S.M., and Zheng, C.Q. 2011. Early Paleoz-
960
oic metamorphic rocks of the Erguna block in the Great Xing'an Range, NE China:
961
Evidence for the timing of magmatic and metamorphic events and their tectonic
962
implications. Tectonophysics, 499: 105-117. doi:10.1016/j.tecto.2010.12.009.
963
Zhou, J.B., Wilde, S.A., and Zhang, X.Z. 2012. Detrital Zircons from Phanerozoic
964
Rocks of the Songliao Block.NE China:Evidence and Tectonic Implications.
965
Journal of Asian Earth Sciences, 47: 21-34. doi:10.1016/j.jseaes.2011.05.004.
966
Zhou, Z.B., Pei, F.P., Wang, Z.W., Cao, H.H., Xu, W.L., Wang, Z.J., and Zhang, Y. 2017.
967
Detrital zircons from late Permian to Triassic sedimentary rocks of Jilin Province,
968
NE China: Constraints on the timing of final closure of the Paleo-Asian Ocean.
Page 45 of 62
969
Journal of Asian Earth Sciences, 144:82-109. doi: 10.1016/j.jseaes.2016. 12.007.
970
Zhu, W., Zheng, B., Shu, L.Ma, D., Wu, H., and Li, Y. 2011. Neoproterozoic tectonic
971
evolution of the Precambrian Aksu blueschist terrane, northwestern Tarim, China:
972
Insights from LA-ICP-MS zircon U-Pb ages and geochemical data. Precambrian
973
Research, 185: 215-230. doi:10.1016/j.precamres.2011.01.012.
974 975
Figure captions
976
Fig. 1. Tectonic sketch maps of NE China, modified from Wu et al. (2007). The inset (a)
977
shows the tectonic setting of NE China. DAK: Dashanzui-Antu-Kaishantun suture belt,
978
GFC: Gudonghe-Fuerhe-Chongjin Fault, and WH: Wangqing-Hunchun suture belt.
979
Fig. 2. Detailed geological map of the southern Yanbian region in eastern Jilin Province,
980
NE China.
981
Fig. 3. Field photograph and photomicrographs of the meta-sedimentary rocks from the
982
Jiangyu Group of the southern Yanbian region, eastern Jinlin Province, NE China (b, e
983
= cross-polarized light; c, f = plane-polarized light). (a) Field location of the
984
biotite-plagioclase gneiss sample HC-1. (b-c) Photomicrographs of the biotite-
985
plagioclase gneiss sample HC-1. (d) Field location of the two-mica schist sample HC-9.
986
(e-f) Photomicrographs of the two-mica schist sample HC-9. Ser: sericite, Bi: biotite,
987
Gt: garnet, Mus: muscovite, Pl: plagioclase, and Qtz: quartz.
988
Fig. 4. Cathodoluminescence (CL) images of selected zircons from the
989
meta-sedimentary rocks of the Jiangyu Group. These zircons were analysed in the
990
present study. Note: Solid and dashed circles represent U-Pb dating and Lu-Hf analysis
Page 46 of 62
991
positions, respectively. The numbers show the ages of the zircons and the ƐHf(t) values,
992
respectively.
993
Fig. 5. (a) U-Pb concordia diagram of all zircon data for sample HC-1; (b) U-Pb
994
concordia diagram of zircon data for sample HC-1 showing the young age population
995
with the weighted mean age of the youngest zircons, which was used to calculate the
996
maximum depositional age; (c) relative probability plot of zircon U-Pb ages for sample
997
HC-1; (d) U-Pb concordia diagram of all zircon data for sample HC-9; (e) U-Pb
998
concordia diagram of zircon data for sample HC-9 showing the young age population
999
with the weighted mean age of the youngest zircons, which was used to calculate the
1000
maximum depositional age; and (f) relative probability plot of zircon U-Pb ages for
1001
sample HC-9.
1002
Fig. 6. Chondrite-normalized REE patterns and upper continental crust-normalized
1003
spider diagrams of meta-sedimentary rocks from the Jiangyu Group in the southern
1004
Yanbian region, eastern Jinlin Province, NE China. The chondrite data are from Sun
1005
and McDonough (1989), and the upper continental crust data are from Rudnick and
1006
Gao (2003). The UCC (Rudnick and Gao 2003) and PAAS patterns (McLennan et al.
1007
1993) are shown for comparison.
1008
Fig. 7. Correlations between zircon Hf isotopic compositions and ages of the
1009
meta-sedimentary rocks in the Jiangyu Group, XMOB: Xing’an-Mongolia orogenic
1010
Belt, and YFTB: Yanshan Fold and Thrust Belt (Yang et al. 2006). The sedimentary
1011
rock data from northeastern Gondwana (i.e. Australia and Antarctica) are from Kemp et
1012
al. (2006) and Ravikant et al. (2011) and the references therein. The data shown in
Page 47 of 62
1013
dashed circles are from Wang et al. (2016).
1014
Fig. 8. Protolith reconstruction discrimination diagrams for meta-sedimentary rocks in
1015
the Jiangyu Group. (a) TiO2-SiO2 diagram (after Tarrey et al. 1976). (b)
1016
Si-(al+fm)-(c+alk) diagram (after Simonen 1953). (c) log(Na2O/K2O)- log(SiO2/Al2O3)
1017
diagram (after Pettijohn et al. 1987).
1018
Fig. 9. Relative probability plot of zircon data from the Jiangyu Group (d), compared
1019
with zircon ages from the eastern XMOB (a), northern NCC (b) and northeastern
1020
Gondwana (c). The data in (a) are from Sun et al. (2013b); the data in (b) are from Sun
1021
et al. (2013b); and the data in (c) are from Rojas-Agramonte et al. (2011).
1022
Fig. 10. Major element discrimination diagrams for meta-sedimentary rocks from the
1023
Jiangyu Group. (a) K2O/Na2O-SiO2 diagram (after Roser and Korsch 1986) and (b)
1024
SiO2/Al2O3-K2O/Na2O diagram (after Maynard et al. 1982). OIA: oceanic island arc,
1025
ACM: active continental margin, PM: passive continental margin, A1: island arc, and
1026
A2: evolved island arc.
1027
Fig. 11. Tectonic setting discrimination diagrams for the meta-sedimentary rocks from
1028
the Jiangyu Group. (a) La-Th-Sc, (b) Th-Sc-Zr/10, and (c) Ti/Zr-La/Sc diagrams from
1029
Bhatia and Crook (1986). The symbols are the same as those in Fig. 10.
1030
Fig. 12. Simplified geological map of the potential positions and tectonic evolution of
1031
the Jiangyu continental arc terrane (modified from Li and Powell, 2001; Wang et al.
1032
2016). NCC: North China Craton, SCC: South China Craton, and JT: Jiangyu
1033
continental arc terrane.
1034
Fig. 13. Simplified geological map of central-eastern Jilin with the locations of the
Page 48 of 62
1035
early to middle Paleozoic igneous rocks along the eastern segment of the northern
1036
margin of the NCC (modified after Han et al. 2018).
Page 49 of 62
Table 1. Comparison of the geochemical characteristics of the Jiangyu Group sedimentary rocks to those of rocks from various tectonic settings Sample
tectonic setting
number
La
Ce
∑REE
La/Yb
(La/Yb)N
∑LREE/∑HREE
δEu
1
Oceanic island arc
9
8±1.7
19±3.7
58±10
4.2±1.3
2.8±0.9
3.8±0.9
1.04±0.11
2
Continental island arc
9
27±4.5
59±8.2
146±20
11.0±3.6
7.5±2.5
7.7±1.7
0.79±0.13
3
Active continental margin
2
37
78
186
12.5
8.5
9.1
0.60
4
Passive continental margin
2
39
85
210
15.9
10.8
8.5
0.56
5
Jiangyu Group
14
31.44
62.41
157.44
9.64
6.92
6.89
0.69
Note: Data for samples 1-4 are from Bhatia (1985). Sample 5 data are averages for the Jiangyu Group.
Page 50 of 62
130°
110° 40
100 140 160
60
180
(a)
(b)
180
Baltic 60 Craton es lid ra U
Omolon Massif and its suroundings
170 60 160
Siberian Craton
Erg
50 150
50
C A O B
40
XMOB
Tarim
Fig.1b
North China Craton 30
Xin
140 30
Tibet block
M una
ass
1
40
Sutures and Faults 1 : Xiguitu-Tayuan 2 : Hegenshan-Heihe 3 : Solonker-Xra Moron - Changchun 4 : Jiayin-Mudanjiang 5 : Yitong-Yilan 6 : Dunhua-Mishan
Russia
n ga
Ma
if
50°
Heihe
if ss
Nadanhada Terrane
SE China
ne Song
To Solonker
n-Zh
130
uan angg
gcai
R
nge
2
Hegenshan
sif M a s Songliao basin ange
r M o ro n 3 Xa
Fig.13
Changchun
i Ra
120
gca
Mongolia
Erlianhot
40°
110
5
uan
100
Jiamusi Massif
4
ngg
45°
90
Zha
80
45°
6 Khanka Massif WH
continental margin accretionary belt DAK GFC
North China Craton
N.Korea 115°
125°
Study area 0
100 200 km
135°
Page 51 of 62
42° 40´
129°30´
+ + + Legend + +++ Cenozoic + + Zhixin +++ P1 Early + + K1 K1 Cretaceous P3 + ++ ++ Late Triassic T3 +++ + + + Early Permian P1 ++ + + + + + + Cpb Carboniferous + ++ + + + + + Cpd + + -Permian + + + + + + + + + + + + + + + Late + + ++ + ++ + ++ + + + + C Carboniferous + + + + + + ++ ++ + + + + + + + + + + 42° + + 35´ + + + C + Jiangyu + + + + + + + + ++ JG + + + Group + + ++ + + + + + + + + + + ++ + + + + Late Permian + ++ + + + + ++ + +++ + ++ + + P3 + utramafic rocks + ++ ++ + + + ++ + + + + + + + T3 + Mesozoic + + + + + + + + + + + + + + granite JG + + + + + + ++ ++ + + + + + + + + + + + + Fault + + + + ++ + + ++ + + + + + + + + ++ + + + + ++ + + + National + + + + + + + + ++ + + + + + + + boundary + + + + + + + + + + + + + + + + + + ++ ++ + + + + + Sample + + + + + + + + + + + + + + + + + + + + + + + + + + + + ++ location + + + + + + + + + + + + + + + ++ + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + ++ + + + + + + + ++ + + + + + + + + + + + + + + + + ++ ++ + + + + + ++ 42° 30´ 129°30´
129°45´
42° 40´
T3 Kedao + + + ++ + ++ + + + ++ ++ +++ + + + ++ +
N
42° 35´
Jiangyu
Beixing
0 129°45´
1
2Km 42° 30´
Page 52 of 62
a
d
HC-9
HC-1
Bi
b
e Mus
Gt
Bi Mus
Pl
Mus Qtz
Qtz
Ser
Qtz Qtz
Mus
Qtz 200µm
200µm
Bi
c
f Gt
Mus
Bi Mus
Pl Bi
Mus Qtz Ser
Qtz Qtz
Mus 200µm
Qtz
200µm
Page 53 of 62
100 µm
(a) HC-1 (+11.5)
(-3.0) 75
63
3
419±7
427±6
451±5
5
31
453±7
1130±21
1770±14
(-6.5)
62
23
29
634±9
42
2591±14
494±8
474±7
(-3.6)
43
32
36
438±5
(+0.8)
563±8
562±6 (+0.1)
19
14
1060±17
(b) HC-9
(+9.9)
1442±46
4
27 (+1.9)
38
2439±12
(-6.9)
(+6.7)
(-7.0)
2658±12 100 µm
29 31
28 37
3
417±6
428±6
(-0.1)
(+5.4)
12
11
27
434±7
(+6.6)
455±7 1843±14
498±7 (-3.0)
70
567±6
613±7
2636±12 66
75
1138±20 933±13
451±4
57
1096±18
15
1648±14
36 (+10.1)
2
2408±12
13 (+1.8)
2926±28
Page 54 of 62
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Page 55 of 62
1000
Sample/Chondrite
(a)
Jiangyu Group PAAS UCC
100
10 La Ce Pr Nd
Sm Eu Gd Tb Dy Ho Er TmYb Lu
10
Sample/ UCC
(b)
1
0.1
Rb Th
K Nb Ce Pr Nd Hf Tb Ti
Er Lu
Ba U Ta La Pb Sr Zr Sm Eu Dy Yb Y
Page 56 of 62
20 D e p le te
Hf(t)
10
(a) d m a n tl
XMOB
e
a .8G
1 t us C r Chondrite
0
ε
Cr -10
-20
Ga
3.
us
500
1000
a
t
Australia
0
0G
t
Cr
YFTB
-30
us
2.5
HC-1 HC-9
2000
1500
2500
3000
t(Ma) 20
D e p le te
Hf(t)
10
XMOB rus
(b) d m a n tl
1.8
t
e
Ga
2.5
C Chondrite
0
ε
Cr
-10
us
3.
0G
a
t
Cr
YFTB
Ga
us
t
Antarctica
-20
-30 0
500
1000
1500
t(Ma)
2000
2500
3000
Page 57 of 62 2.0
(a)
Jiangyu Group
TiO 2 (wt.%)
1.5
Sedimentary rocks
1.0
Igneous rocks 0.5
0.0 40
50
70
60
90
80
SiO 2 (wt.%) 70
(b) Pelite
(al+fm)-(c+alk)
60 50 40 Sandstone 30 Volcanics
20 Carbonate
10
sediments
0 0
100
300
200
400
500
Si
(c)
0.5
it e Quart
Arkose
z aren
Sub
-0.5
a r e n it e
ark
th
0.0
S u b li th
ar
ose
en
ite
Graywacke
Li
log(Na 2 O/k 2 O)
1.0
-1.0 0.0
0.5
1.0
log(SiO 2 /Al 2 O 3 )
1.5
2.0
Page 58 of 62 (a) Relative probability
Eastern XMOB N=662
(b) Relative probability
Northern NCC N=347
Relative probability
(c)
1860
NE Gondwana N=176
590
2520
970
Relative probability
(d)
455 Jiangyu Group N=186
428 476 564 622 9351124 200
1676 1979 2288 2649 1816 2423 2926
600 1000 1400 1800 2200 2600 3000
Age(Ma)
Page 59 of 62
100
(a)
江域岩组
K 2 O/Na 2 O
10 PM 1
ACM
0.1 OIA 0.01 40
50
70
60
80
90
SiO 2 (wt.%) 10
(b)
江域岩组
SiO 2 /Al 2 O 3
8 ACM
6
PM
4
2 0 0.01
A1
0.10
A2
1.00
K 2 O/Na 2 O
10.00
100
Page 60 of 62
Page 61 of 62
(a)
late Neoproterozoic SCC
Tarim JT NCC
Paleo-Pacific Ocean
Gondwanaland
early Ordovician
(b) NCC Paleo-Asian Ocean
JT
scc Paleo-Pacific Ocean Tarim
Gondwanaland
late Silurian- early Devonian
(c )
Paleo-Pacific Ocean Paleo-Asian Ocean JT
NCC
SCC
Tarim
Gondwanaland
Page 62 of 62
124°
125°
126°
127°
128°
129°
Legend + + Permian-Jurissic intrusive rocks
SXCYS-Solonker-Xar Moron-Changchun-Yanji suture YYF-Yitong-Yilan fault DMF-Dunmi-Mishan fault KSF-Kaiyuan-Shanchengzhen fault 44°
SX
Changchun CY
biotite schist 414-457 Ma Jiang et al. 2014
granodiorites 414&419 Ma Pei et al. 2016
S
acidic ignimbrite 392-449 Ma Jiang et al. 2014
Y
F
124°
+
125°
Early-middle Paleozoic igneous rocks
Y Jilin
DM Jiaohe
tonalite 443 Ma Pei et al. 2016 meta-diabase
+ +493+Ma + Pei+et+al. 2016 + ++ + monzogranite ++ ++ + + ++ 400 Ma + ++++ Pei et al. 2016 + + + Siping + + + + + + + + + + rhyolitic tuff + + + + + + + + + + + 410&403 Ma + + + + ++ + + + + + + + + +Pei + et al. +2016 + + ++ + + + + + + + + + + + + ++ + + ++ + + 43° ++ +++ ++ + + + + ++ + + + + + + + + + + Huadian + + ++ + + + + + + + + + + + + + Panshi+ + + ++ +++ ++ + + + + + +++ + monzogranite + ++ ++ + ++ + + + + + + + + + 396 Ma + ++ + Kaiyuan + + Pei+et al. 2016 + + + + + + + ++++ ++ ++ +++ + + ++++ ++ ++ +++ + + ++ +++ ++ ++ + ++++ ++ + K S+F+ rhyolitic rocks 390&425 Ma Han et al. 2018
Permian-Early Triassic mélange
metarhyolite 360Ma Wang et al. 2015c
126°
127°
F
++
+++ ++ ++ ++++ ++ + + Dunhua ++++ + ++ + ++ ++ + +++++ ++ + + + + + + +++ +++ ++ + + + + + + + ++ +++ + + + + + + + + ++ + + + + +++ + + + + + + + + + + ++ + + + + ++ + + + +++++ ++ +++ + + + ++ + + + +++++ ++ ++++ ++ + +++ ++ ++++++ + 43° + + ++ + + +++ ++ Yanji + + + + + + + + + ++ + + + + ++ + + ++++ + + + + tonalites Hunchun ++ ++ + + 422&423 Ma + + + Wang et al. 2016 ++ + + + ++ + + + ++ ++ + Helong + + ++ + + + ++ + + + ++ ++++ + Jiangyu + + ++ +++++++ Group ++ ++++++ ++ +++ + ++ 0 10 20km ++
128°
129°
130°
131°