Subduction, collision and exhumation in the ultrahigh-pressureQinling - Dabie orogen

BRADLEY R. HACKER I, LOTHAR RATSCHBACHER2 & J. G. LIOU3IGeological Sciences, University of California, Santa Barbara, CA 93106, USA

2lnstitut fiir Geologie, Technische Universitiit Bergakademie Freiberg,Freiberg, D-09599, Germany

3Geological and Environmental Sciences, Stanford University,Stanford, CA 94305, USA

c':. Abstract: High-pressure metamorphism and ophiolite emplacement (Songshugou ophio-lite) attended suturing of the Yangtze craton to Rodinia during the c.l.O Ga Grenvillian oro-

. geny. The Qinling microcontinent then rifted from the Yangtze craton at c.750Ma. The.;~ Erlangping intraoceanic arc formed in the Early Ordovician, was emplaced onto the Qinling, microcontinent in the Ordovician-Silurian, and then both units were accreted to the Sino-

Korea craton before being stitched together by the c.400 Ma Andean-style Qinling arc.Subsequent subduction beneath the Qinling-Sino-Korean plate created a Devonian-Triassic accretionary wedge that includes eclogites, and formed a coeval volcano-plutonicarc that stretches from the Longmen Shan to Korea. In the Late Permian-Early Triassic,the northern edge of the South China Block was subducted to > 150 km depth, creating thediamond- and coesite-bearing eclogites of the Dabie and Sulu areas. Exhumation fromthe mantle by lithosphere-scale extension occurred between 245 and 195 Ma during clock-wise rotation of the craton. The Yangtze-Sino-Korea suture locally lies tens of km north ofthe exhumed UHP- HP part of the South China Block, implying perhaps that the very tip ofthe South China Block was not subducted, or that the UHP-HP rocks rose as a wedge thatpeeled the upper crust of the unsubducted South China Block from the lower crust. The Tan-Lu fault is an Early Cretaceous to Cenozoic feature. The apparent offset of the Dabie andSulu UHP terranes by the Tan-Lu fault is a result of this Cretaceous to Cenozoic faultingcombined with post-collisional extension north of Dabie.

The Sino-Korean craton and the Qinling micro- basement outcrops can be assigned either a Sino-3. continent colli~ed in the Ordovician-Silurian. Kore;an or Yangtze crat.on affini~y, where~s the~,., The North China Block (NCB) and the South affinIty of areally extensIve domaIns of sedImen-

~ China Block (SCB) collided in the Permo-Triassic. tary strata or of volcano-plutonic complexes can1,4 The orogenic belt associated with these collisions be ambiguous. 'North China Block' and 'South"f);' and intervening tectonism extends c.2000 km China Block' are used to refer to the continental

west-east through the Qinling, Tongbai, Dabie blocks north and south of the Qinling-Dabie-Shan and Sulu areas and into Korea (Fig. 1). It is Sulu suture.of special interest because it contains high-pressure The Sino- Korean craton is subdivided into(HP) rocks of four different ages: Grenvillian, three units: the western, eastern and centralDevonian, Carboniferous and Triassic. This paper blocks. The western and eastern blocks areaims to provide a review of the collision zone as Archean cratons linked by a central suture beltboth a summary of what conclusions have been that formed during collision at c.1.8 Ga (Zhaodrawn where and with which data, and as a guide et at. 2000). The U-Pb zircon ages from theto future reseal\;h. Sino-Korean craton cluster at c.3.8, 3.3, 3.0, 2.5

and 1.7-1.8Ga (Song et at. 1996; Yu et at.. 1996; Zhao et at. 2000). The craton consists of

Smo-Korean craton a basement of Archaean to Proterozoic meta-

In our usage, the Sino-Korean and Yangtze cra- morphic rock overlain by a relatively uninter-tons comprise Precambrian basement and cover rupted 4-8 km thick superjacent section ofas described below; in principle, all Precambrian Sinian (Late Proterozoic to Early Cambrian) to

From: MALPAS, J., FLETCHER, C. J. N., ALl, J. R. & AITCHISON, J. C. (eds) 2004. Aspects of the Tectonic Evolution ofChiua. Geological Society, London, Special Publications, 226, 157-175.0305-8719/04/$15 ((;) The Geological Society of London 2004.

1 ! ! ii , .

thrust fault

Lushi

Tan-

Lu fa

ult

J2

30o

113o

Xi'an

Lo-Nan F.

Lu Shan

Shanyang

Danfeng Shangnan

O

111o

35o113o

35o

115o

contact, depositional or intrusive

faultinferred contact

structural trend

antiformsynformhomocline

Triassic sedimentary rocks

post-Triassic rocks

Cretaceous plutons

Triassic plutons

Paleozoic plutons

33o

Queshan

Shiyan

Fangxia

T3

Shang-Dan F.

Shan-Feng F.

Wudang Shan

Wudang F.

Gonglu F.

Zhuqi F.

J2

J3

Huangling

Shennong

T1

S

T1

Wuhan

J3

Meishan Fm.

Xinyang

NanyangBasin

Erlangping

unit names are italicized

Qinling

Kuanping

Kuanping

Foziling

P

J1

J2

P2

T3J1

P2

Explanation

100 km

32¡

109¡

33o108o

31¡

111¡

Sino-Korean craton cover and basement; letter shows age of youngest rocks

Douling

Songshugou

Liuling

Wudang &Yaolinghe

Suixian &Yaolinghe

Xiaomoling

Heihe

Guandaokou

Xiong'er

Xiong'er

Taihua gneiss

Lu Shan fault

T

J1

T3

Dengfeng

Xinyang

N

Shagou F.Chenhe F.

C

coesiteeclogite

blueschist

blueschist

amphibolite

quartz eclogite

NorthernOrthogneissCretaceous Xiaotian-M

ozitan fault

Kuanping unit

Erlanping unit

Qinling unit

Songshugou ophiolite

Douling, Sujiahe (incl. Huwan), Luzhenguang unit

Liuling unit

Yangtze craton cover and basement; letter shows age of youngest rocks

Luzhenguang

Triassic high-pressure and ultrahigh-pressure rocks

coesite eclogite

quartz eclogite

eclogite → amphibolite

blueschist → greenschist

XinyangHuwan shear zone

eclogite

Songxian

Dengfenggreenstone

M301,247B297,264

K205±5Z404,780,1.0,1.545

H152 or K?45

B10145

K9545

K~1000→22045

H~100045 M806->75045

H23745

M232→15045

K100-105

2.814

Pb2.514

K55

H4347

H4337

H3167 H1357z746, 77612 H40113

m450,4339

H<498 K100, 6026

H4047

H400→222M22713M243,26613

B12013Z6562

Z2.02

Z1.52

b1213

b1243

b4303

b3893

b1353

b3413

b1403

b1353

Rb1058

KAr7188

Rb1434

Ar2144

Ar2174

Rb4184Z2004

Z7254 z1.7Sm1.9Sr422H83316

Srwr9919

M2321

B3141B327 M3481

rieb2161

KAr4072

KAr4852

KAr1312KAr1402

KAr1412

KAr3842H402K~20045

KAr3982

KAr8802

KAr3702

KAr1272KAr1002

KAr1032

KAr7952

Z7472

Z74515

0.9(15)

0.9(15)

Rb2.82

Rb2.62UPb2.42

Z2.62

z7625

z0.8,2.613

Z77826

Z77125

Luzh sed: Pb734-1.949Foziling granites: Z719-76649Foziling sed: Pb 2.5, 1.9-1.8 Ga, 1.0-0.7 Ga, 455 Ma49

K~1000→25045

Yang

tze

crat

on (S

CB

)Si

no-K

orea

n cr

aton

(NC

B)

reference

K205[c. 870]*

age (Ma)

K: 40Ar/39Ar K-feldsparB: 40Ar/39Ar biotiteM: 40Ar/39Ar K-white micaH: 40Ar/39Ar hornblendeb: K/Ar biotitem: K/Ar K-white micah: K/Ar hornblendeZ: U/Pb zirconRm: Rb/Sr whole-rock-K-white micaRb: Rb/Sr whole-rock-biotite

zircon core (if present)Geochronology Explanation

location

Sm2248

Z76125

Z~75044

M235,K20526

M220→25617

M20533

m186, 2289m196,2039

m2159

Z22732

~2.9, 2.9-3.3 (19)

Ar4218

Z3912

Z226,85422

M18028

K17133

M225, 22218

z470, 43513

Rb40210

coesite

coesite

eclogite

Huwan shear zone

Z77926

Z23221

M23018

M21318

M23617

M21417

M19518

M23323

Sm44643 M23017Z660,73526

M26317

M23133M22433

M21233

M2473324917

M23433

M196,22233

M23433

M20733M20533

K16933

m2079

M19017

m2329 b2269

m1979

m201,2059

M20118M19833

M19533

M19633 M23733

M~400x217Z312[~400]21

Z3072Z311,307[433]21

Z400H399?39Sm42240

Foziling

quartz eclogite

eclogite

Z73926

Z78126

Sm2448Sm23136

Sm22836

Z79825

Z67422

Z76825

Z1.329 Z2.129

Z6382277231

Z75729

Sm23842

Sm21048

Z229[707]46

M17926

B~197,M20826M2161

M196 K20424

B22724

M1951

M22124

m2109

M1787M19128

Z22425

K22025

M21825

M24226Z667,73926

H742,77026

K18026

m2139

m2259

m2029

b204, 2239

M20624

M210,19826

H28026

Z87025

coesite

Z21822

NorthernOrthogneiss

Sm20848

M185,H21427

Sm218-210 x6,Rm 223-19830

Rbb194,194,197,198,198M205,206,206,212B201,202,211,21035

Z218-240,K203,B199,216,M195,H195(?)24

Z21422Sm246,Rb24023H22524Z21829

Z223[1.8]41

Rm23623M19024K176,M183,19026Z238[1.9]mz223,20934Z233[2.5]Sm23135Sm226x2,Rbb169,171,173,174,18137

Z77231Sm22136Z227,B19022

M200B19024,B195,K19526

b182,216,2319 Z21829

Z230,mz20934

G

G B A IH

D A B I E

S H A N

O N G 'A N

T O N

QI

NIL

N

Songshugou

H42045Sm98347m4253

m3543

Ar4218

Rb3838

Rb6704

Rb4444

Rbwr4529

Rbwr4249 Rbwr9919

Rbwr7949Rbwr9739

Rb4864

KAr4012KAr3802

KAr4032

KAr3942

KAr4802

Z3912

H~400K22045

K23045 z488,4875

Z43720

b4323

KAr3702

coesite eclogite(Hu et al.,1995)

northern Liuling=Qinling(?)

z4805

Rbwr40211

Sm40038

m4203

KAr4022

H³386K27045

quartzeclogite

eclogite→amphibolite

Z78125

Dengfeng greenstoneTaihua gneiss

Xiong'er &GuandaokouGroups

2.5-2.8Ga

OrdovicianthruSinian

Silurianvolcanism

Lower CarboniferoustoUpper Ordovician

tectonichiatus

platform

PermianthruDevonian

Devonianclastics (partlydeep marine)

Lower Triassiccoal andphosphorite

shallow marine-lacustrine

4Ð8

km

basement

basement

MesozoicthruEarlyTriassic

continentalcontinental

unstable shelf

lacustrine to alluvial

middle Carboniferous-Early Permian andesites

+crustal derivedJurassic volcanics

Sino-Korean craton Kuanping: Sino-KoreanPr oterozoic-Silurian

passive margin/accr etionary wedge(?)

pre-EarlySilurianparagneissbasement

~638Madetrital zircon

PermianthruMiddleCarboniferous

amphibolite-greenschist~435 Mametamorphism

Erlangping-Danfeng-Heihe

intraoceanicarc

oceanicsediments

up to~420 Ma

pillowedvolcanics &sheeted dikes

older than~480 Ma

plutons490-470 Ma

~490-470 Maintraoceanic arc

~440-390 Ma Qinlingarc and arc metamorphism

=Kuanping(?)

Qinling: Sino-Koreancover, ophiolite andYangtze basement

subduction(~490-470 Ma)

435-470 Masubduction and collision(?)

subduction ³400 Mano collision

Grenville (~1 Ga)formation ofRodinia

South China Block

Devonian-Permian(?)flysch and molasse

=Qinling(?)

=Yangtze craton(?)

Southern Liuling:Paleozoic

flysch and molasse(?)

Northern Liuling: = Qinling(?)

Douling: Yangtzebasement

Yangtze craton

Devonian-Permian(?)siliclastic &volcaniclasticrocks

amphibolite,marble, gneiss

~400Macontactmetamorphism ~310 &

400 Ma(?)eclogite

orthogneiss,acid todominantlyTi-richpillow basalt

0.7-0.8 Ga

Upper Sinianto Lower Triassicplatform carbonateson passive margin

Upper Triassicclastics

Lower-Middle Triassicevaporite,carbonate &breccia

pre-~435Maaccretionary wedgeor passive margin

amalgamated by 400 Ma

Yan

gtz

e ri

ftin

g

Yan

gtz

e ri

ftin

g

Mesozoic evolution sameas Sino-Korean craton

Triassic HP-UHP metamorphism(245-220 Ma)

paragneiss&amphibolite

coesiteeclogite

2.1-2.6 Ga670-990 Ma

400 MaSongshugouophiolite

~1 Ga

marble,

Up

per

Qin

ling

Low

er Q

inlin

g

paragneiss,amphibolite

craton

relict eclogite

North South

(southern margin) (northern margin)

~12 km

suture

sutu

re

sub

duc

tion

zon

e

sub

duc

tion

zon

e

sutu

re

North China Block South China Block

Figure 3: Geologic units, tectono-thermal/sedimentary events, facies interpretation, radiometric ages, and tectonic interpretation of the Paleozoic-early Mesozoic Qinling orogenic belt. Formation of the intra-oceanic Erlangping arc between ~490-470 Ma was followed by accretion of the lower Qinling micro-continent to the intra-oceanic arc, and to the Sino-Korean craton. Subduction underneath the northernmost Liuling unit imprinted the ~400 Ma Qinling arc on the Sino-Korean + Qinling collage. A subduction signature is again evident during the mid-Carboniferous to Late Permian on the Sino-Korean craton, when the Paleo-Tethys was subducted northward, producing the andesitic magmatism on the Sino-Korean craton. In the Late Permian-Early Triassic, the leading edge of the Yangtze craton was subducted to >150 km and subsequently exhumed by crustal extension (after Ratschbacher et al. in press).

Tan-

Lu fa

ult

J2

30o

113o

Xi'an

LoÐNan F.

T

O

111o

35o113o

35o

115o

33o

T3

ShangÐDan F.

ShanÐFeng F.

Wudang F.

Zhuqi F.

J2

J3

T1

S

T1

Wuhan

J3

NanyangBasin

Foziling

P

J1

J2

P2

P2

32¡

109¡

33o108o

31¡

111¡

D a b i e S h a n

H o n g ' a n

T o n g b a i

Q i n l i n g

Douling

Liuling

Kuanping

Guandaokou

XiongÕer

XiongÕer

Taihua gneiss

Lu Shan fault

T

J1

T3

N

Shagou F.Chenhe F.

C

Cretaceous XiaotianÐMozitan fault

Luzhenguang

Xinyang Huwan shear zone

Figure 4: Major units and unit boundaries of the Qinling-Dabie orogen (see Figure 2 and its caption).

southern limit of NCB/northern limit of Yangtze affinity rockssouthern limit of Devonian tectonism

northern limit of Triassic metamorphism

northern limit of Triassic exhumation

southern limit of Sino-Korean cratonErlangping Intraoceanic Arc

Wudang ShanCore Complex

Hong'anHP-UHPTerrane

Dabie HP-UHPTerrane

Lower Yangtze fold-thrust belt

Yangtze craton basement and cover

Sino-Korean craton basement and cover

Qinling Microcontinent

. 1

162 B. R. HACKER ET AL

North China Block-South China Block suture in NCB (Yin & Nie 1993). This intra-oceanic arcthe Hong'an-Dabie areas. can be traced eastward as far as Hong'an,

High-pressure metagabbro, amphibolitized where it disappears beneath Cenozoic sediments~clogite and felsic granulite associated with (Figs 2 and 4). No such ophiolite is known fromc.l.0-l.2 Ga ophiolitic rocks were emplaced on Sulu or Korea, but there are several candidatestb the lower part of the Qinling unit in the Song- for Palaeozoic ophiolites in the Kunlun-Altynshugou area, following high-pressure meta- Tagh-Qaidam-Qilian area (Matte et al. 1996;morphism in an oceanic setting (Liu et al. Sobel & Arnaud 1999).1996; Song et al. 1998; Zhang 1999). The amphi-bolitized eclogite was derived from MORB, is in S"l. E I D . Q. I.fault contact with mantle peridotite and contains I unan- ar y evoman In mg arc

4ecompression textures common in many eclo- Following emplacement of the Early Ordoviciangites, including symplectites of plagioclase and Erlangping intra-oceanic arc, a continental mar-diopside derived from omphacite estimated to gin arc was built on the Kuanping, Erlangpinghave formed at pressures ~ 1.5 GPa (Zhang and Qinling units from c.438-395 Ma; this1999). A Sm-Nd mineral isochron of 983 Ma implies that the Erlangping and Qinling units'is taken to date later cooling. The high-P felsic were amalgamated with the Kuanping unit (andgranulite includes garnet + kyanite + micro- thus the Sino-Korean craton) prior to c.440 Maperthite + quartz + rutile assemblages formed (Fig. 3) (Ratschbacher et al. in press). Signifi- ;.at 800-900°C and 1.3-1.6GPa (Liu et al. cantly, none of these Silurian-Early Devonian1996). plutons crop out within the Liuling unit. How-

Palaeoclimatic, palaeobiogeographical and ever, the northern part of the Liuling unit,palaeomagnetic data imply that the North China which Ratschbacher et al. (in press) correlatedand South China blocks were close to or part of with the Qinling unit, experienced the regionalnear-equatorial East Gondwana through the contact metamorphism produced by this batho-Late Devonian, and that rifting of the NCB lith, and Silurian to Lower Devonian strata int1rom Gondwana took place after the Devonian the northern Liuling unit received metamorphic~hao et al. 1996; Huang et al. 2000). detritus (Mattauer et al. 1985) from the Qinlingi arc and c.780Ma and c.l.0Ga detrital zircons

(see above). We thus interpret the southernOphiolites and accretionary complexes NCB, and units as far south as the northern

Liuling unit, as having been stitched togetherEarly Ordovician Erlangping Ophiolite, the by the 400 Ma magmatic-metamorphic event,Qinling Microcontinent and their and suggest that an Andean-type continental

... margin arc was built along the southern marginamalgamanon wIth the SIno-Korean Craton of the NCB at this time; we place the subduction

The distribution of ophiolites within the Qinling- zone producing the Silurian-Devonian arcDabie-Sulu orogen provides important infor- south of the northern Liuling unit (Ratschbachertpation about the (partial) closure of ocean et al. in press). The local absence of Upper "basins. The oldest Palaeozoic orogenic event in Ordovician (c.445 Ma) through Lower Carbon-~e Qinling orogen was the formation of the iferous (c.350 Ma) rocks from the NCB in the~rlangping intra-oceanic arc, which includes Qinling orogen probably reflects uplift related l'

the Heihe, Danfeng and Erlangping units to the formation of this Andean.style Qinling arc.(]Fig. 3). Sediments associated with the arc contain High-pressure rocks that may be associatedCambrian-Ordovician through Ludlovian- with the Qinling arc have been found by HuWenlockian (419-428 Ma) radiolaria, and tron- et al. (1995, 1996) in the northern Qinling areadjhemites, tonalites, gabbros, and rare pyroxenites (Fig. 2, offset). Hu et al. reported lenses andwith single-zircon PbjPb ages of 470-488 Ma blocks of eclogite, coesite-bearing eclogite andthat intrude a volcanic sequence (see summary retrogressed amphibolite within garnet-bearingin Ratschbacher et al. in press). Ratschbacher quartz and phengitic mica schist. While the indi-8t al. (in press) proposed south-directed emplace- vidual outcrops are no more than a few metresment of this arc on to the lower Qinling unit (the wide, the belt of eclogites eJ(tends more than~inling microcontinent) between c.470 and 10 km (Fig. 2). The eclogites c~nsist of garnet +435 Ma, based on the present geographical pos- omphacite + rutile + quartz + zoisite :t phengiteitions of the arc, the upper Qinling unit and the (3.5 Si atoms per formula utrit):t amphibole;lpwer Qinling unit. The Erlangping-Qinling col- many have been extensively retrogressed.lision may have been related to the collision of the Inclusions of coesite and its pseudomorphs inPamir-South Tarim-Qaidam continent with the garnet and omphacite were identified in a few

Ii

SUBDUCTION, COLUSION AND EXHUMATION 163

samples, based on optical properties and the of California (Ye et al. 1994; Liu et al. 1996).presence of radial fractures around the inclusions; They have yielded SHRIMP U - Pb zircon agesthis identification, however, should be confirmed of c.310 Ma (Sun et al. 2002), 400 Ma (Jianby Raman spectroscopy. Pressure-temperature et al. 1997), a Sm/Nd isochron of 422 Maestimates based on mineral composition range (Li et al. 1995), an amphibole 40 Ar /39 Ar age offrom 1.3 to 1.5GPa and 590 to 758°C; coesite 400Ma (Jian et al. 1997), and a muscoviteof course would indicate P> 2.6 GPa. A Sm- 4OAr/39Ar age of 400Ma (Xu et al. 2000a).Nd isochron for gamet, omphacite, rutile, amphi- Sun et al. (2002) directly tied their c.310 Mabole and whole rock is reportedly 400:t 16 Ma age to high-pressure recrystallization with laser(although we are unable to reproduce this age ICP-MS trace-element analyses that demon-from the reported isotopic ratios). strated zircon growth while garnet was stable

The Qinling continental arc can be traced east- and plagioclase was not stable.ward as far as Hong' an, where it disappears During and after the formation of the Qinlingbeneath Cenozoic sedimentary rocks (Figs 2 Andean-style volcano-plutonic arc, the southernand 4). No such arc is known from Sulu or margin of the NCB was dissected by sinistralKorea, but possible correlatives exist in the Kun- wrenching along the Lo-Nan and Shang-lun Mountains of northern Tibet (Matte et al. Dan shear systems at 420-380 Ma (Fig. 2)1996; Yang et al. 1996). (Ratschbacher et al. in press). We assume that

oblique subduction imposed these spectaculartransDressive wrench zones. Muscovite and bio-

Devonian- Carboniferous accretionary wedge tite 4t> Ar /39 Ar ages ranging from 348 to 314 Ma

A probable fossil accretionary complex, also with have been interpreted to reflect a continuationhigh-pressure rocks, lies south of the Silurian- of this strike-slip motion into the Permian (Mat-Earl~ Devonian arc in the Liuling and Sujiahe tauer et al. 1985). On a larger scale, the NCBunit$ (Fig. 3). The Liuling unit is a mixture of and SCB rifted from Gondwana in the Latesiliciclastic and volcaniclastic rocks, amphibolite Devonian-Early Carboniferous (Li & Powelland minor carbonate (You et al. 1993). Correla- 2001).tive rocks include the Xinyang Group in Tongbai-Hong'an and the Foziling unit in Dabie. . .. .pevpnian fossils in the Tongbai area (Du 1986; Devoman-Tnasslc volcano-plutonIc arcNiu' et al. 1993) have been used to infer a It is unclear whether the inferred Devonian-Per-Devpnian age for the entire Liuling; however, mian subduction beneath the NCB produced at:lu and Meng (1995) showed that several continental margin arc. Younger, Permian andconglomerate-bearing, volcaniclastic deposits, Triassic metaluminous, probably I-type plutonslocally containing metabasalts and metacarbo- with low Sri ratios (Xue et al. 1996a) intrudenates, have proven Upper Devonian and Lower the Kuanping, Erlangping, Qinling and LiulingCarboniferous and suspected Carboniferous to units as far east as Xi'an (Figs 2 and 4). CoevalPermian ages. The Sujiahe unit mainly contains intrusions pierce the western edge of the Yangtzevolcaniclastic rocks and 'melange' (Ratschba- Craton in the Xue Shan, Longmen Shan, thecher et al. in press). Songpan-Ganze flysch and the SCB cover

Blocks of eclogitic rocks and retrograde south of the Qinling mountains (Fig. 1, Regionalamphibolites occur in a shear zone 1-3 km Geological Survey of Gansu 1989, Regionalwide near the southern edge of the Sujiahe unit Geological Survey of Shaanxi 1989). The plutons5 - 20 km northwest of Tongbai. The eclogites intruding the SCB cover raise an important pro-con~ain gamet, omphacite, quartz, rutile, phen- blem, as they appear to be south of the inferred~iteand barroisitic amphibole, and have yielded north-dipping subduction zone. East of Xi'anP-T estimates of 480-550 °C and 1.3-1.8 GPa this arc may end, disappear under Cenozoic sedi-twe~ et al. 1999). Ye et al. (1994) reported Sm- mentary rocks, or be covered by younger thrustNd tnineral/rock isochrons of 533 :t 13 Ma and slices. Middle Carboniferous to Early Permian$44114 Ma and a 40 Ar /39 Ar barroisite age of andesites form a NE-trending belt across the east-

399:it4 Ma. This belt of HP rocks in the Sujiahe em half of the NCB (Fig. 1) (Zhang 1997), butunit extends as far east as the Xiongdian area of the belt is surprisingly far north of and obliqueHong' an, where eclogite lenses or layers crop to the inferred NCB-SCB suture.put jn quartzite and felsic gneiss. These eclogites We suggest that the pre-collisional, Permo-con~ain minor glaucophane and phengite in Carboniferous NE trend of the NCB-SCB sutureaddition to gamet, omphacite and rutile, and in Tongbai-Hong'an-Dabie and the suture-arcfonned at Po::: 1.3-1.5 GPa, To::: 590-680°C, distance were modified by the Triassic, syn-similar to tectonic blocks in the Franciscan Complex collisional clockwise rotation of the SCB

-

SUBDUCTION, COLLISION AND EXHUMATION 165

(Wei et at. 1998; Tsai & Liou 2000; Xu et at. only 400-800 MPa at 350-450 DC (Eide & Liou2000b; Zhou et at. 2000; Liu et at. 2001); (3) 2000). While most of the evidence of UHPthe Zhangbaling and Bengbu areas, a mostly derives from eclogites, the paragneiss also con-blueschist-facies extensional complex (our obser- tains local unambiguous indications of meta-vations); and (4) the Sulu area (Wallis et at. morphism at similar pressure and temperature,1999) (Fig. 1). such that the eclogites clearly were metamor-

The evidence of Triassic HP and UHP meta- phosed in situ (Liou et at. 1996), the same maymorphism comes chiefly from a few per cent of not hold true for ultramafic blocks, some ofeclogite and garnet peridotite boudins that are which record recrystallization pressures >4 GPahosted by paragneiss plus less granodioritic- (Okay 1994; Hacker et at. 1997; Liou & Zhangtonalitic orthogneiss (Fig. 6) (Cong 1996; Liou 1998). The spatial distribution and metamorphicet at. 2000). The highest temperatures and press- conditions of these: HP through UHP rocksures attained in the coesite- and, locally, diamond- indicate subduction~zone metamorphism on abearing Dabie eclogites were 825-850 DC and regional scale.3.3-4.0 GPa (Carswell et at. 1997). The coesite- The age of UHP metamorphism in the Dabie

~ free eclogites reached somewhat lower peak Shan is now well constrained to be Middle-

conditions of 625-700 DC and 2.2-2.4 GPa in Late Triassic (e.g. Hacker et at, 2000). Thethe Dabie Shan (Okay 1993; Liou et at. 1996; most recent data indicate that UHP recrystalliza-

~ Carswell et at. 1997), and have been divided tion may have begun as early as 245 Ma andinto kyanite-bearing and kyanite-absent eclogites extended through c.225-230 Ma (Okay 1993;in Hong'an, with estimated physical conditions of Hacker et at. 1998; Hacker et at. 2000; Li et at.550-650 DC, 1.6-2.5 GPa and 450-550 DC, 2000; Chavagnac et at. 2001; Ayers et at.0.8~1.2GPa, respectively (Eide & Liou 2000). 2002). High-pressure rocks in Hong'an (theThe amphibolite unit is a hornblende-rich orthog- area least affected by Cretaceous reheating) indi-neiss; peak pressure and temperature estimated cate that the regional amphibolite-facies over-from one locality are > 1.0 GPa and :::: 650 DC (Liu print at 500-650 DC and 0.8 GPa occurred during& Liou 1995). Blueschists reached conditions of the 195 - 225 Ma time span (40 Ar /39 Ar phengite

I!,i

i, Eclogites Garnet peridotites8 7Dable -5ulu te"ane , Dabie-5ulu terrane

I. Eastern Dable ,II. Central Dabie " @Mantle-derIVed spinelIII. Yangkou Beach, 5ulu, @peridotlte (5) and ' , "IV. Weihai 5ulu ' 6 G garnet peridotite (G) ,, , G

5 NQ: North Qinling ,'UHP . Crustal maflc-ultramsfic b

HW H ' complex c~: uwan .,. , ~"" ~ej,. , ,%0" ~'(',- 5 ~"~,- 4 ov, ,/~ - ~, DryEC

tV '-Q. ,.

. ,(!) Lw-EC ,--, 4 'GI' """, ,~ 3 ' "

, m,' "/j GI '... 3,'-

I Q. ,i ,,' ~\e

2 " "

2 .j,"I ~<;,-" ~o\\\8

~ II1

0 0200 400 600 600 1000 200 400 600 1000 1200 1400

Temperature °C km-1

Fig. 6. Metamorphic pressures and temperatures for eclogites and peridotites of the Qinling-Dabie-Sulu orogen(modified after Liou et ai. 1999; Zhang et ai. 2001).

,h

L _I l" "...

'I IiI\ill I,

166 B. R. HACKER ET ALI,: ages). ~ost o.f the ~-f:ldsrar 40 Ar/~9 Ar spectra exten.sional exhumation of the HP- UHP rocksi have mflectIons mdicatmg cooling below remams unclear.I c.200 °C near 170 Ma, although some rocks were The HP to UHP rocks of Dabie- Hong' an are

this cool as early as 200 Ma. Such P- T paths, mostly a structural homocline with SE-dippingwith concomitant decompression and cooling are foliation, SE-plunging lineation, and overall

.. only possible if exhumation was rapid or the slab top-to-NW flow that includes significant coaxialwas refrigerated by deeper level subduction stretching (Fig. 7). In northern Hong' an, how-(Hacker & Peacock 1995; Ernst & Peacock ever, the S-oriented structures rollover through1996). The exhumation rate is only crudely con- horizontal into a 5-km-thick zone of N(W)-dip-strained to c.3-l5 mm/year. ping foliations, N(W)-plunging lineations, and a

" Geochronology shows that the Middle-Late N(W)-directed sense of shear. This, the HuwanTriassic thermal event associated with the UHP shear zone (Webb et at. 2001), effectively strad-metamorphism in the eastern Dabie Shan and dIes the Triassic suture. It developed out of theHong'an areas extended as far north as the high-strain gneisses of typical Yangtze affinity

i Erlangping unit in the Qinling area, the Xinyang in northern Hong'an, contains strongly retro-, 6 unit in the Tongbai and Hong'an areas, and the gressed eclogite boudins of pre-Triassic age ini .. Foziling and Luzhenguang units in the Dabie the Sujiahe complex (see above), and dies out

r Shan (Hacker et at. 1.998; Hacker et at. 2000). northward in the phyllitic quartzites typical ofThe absence of HP metamorphism means that the southern Liuling unit. The Huwan shearthese northernmost units were not subducted zone can be followed - with interruptions by Cre-during the collision, but the Late Triassic meta- taceous plutons - into northern Dabie, where it ismorphism is certainly related to the collision. truncated by a large Cretaceous pluton. The pseu-

dostratigraphy of the Hong'an area also defines aseries of kID-scale NW -trending synforms and

t . .. antiforms that are overturned to the north in cen-Co uslonal defonnatlon tral Hong'an, and are upright to south facing in

The Triassic NCB-SCB collision produced a southern Hong'an. The coesite-bearing eclogitedistinct set of structures throughout the Qinling- unit forms the core of the northernmost antiform;Dabie orogen: NW-SE to N-S contraction by the lowest pressure rocks, blueschist, are presentfolding and thrusting Ithroughout the belt, sub- only on the south limb of this orogen-scale fold.horizontal NW -SE to N -S extension within The westward decrease in peak metamorphiccore complexes along the northern margin of pressures reveals that the antiform plungesthe South China Block, and dextral transpressive west. This antiform extends eastward intoreactivation of existing shear zones in the Qinling Dabie where it is partially overprinted by thearea (Fig. 5). dominantly Cretaceous intrusions and structures

The UHP rocks in both Dabie-Hong'an of the Northern Orthogneiss (Ratschbacher et at.(Faure et at. 1999; Hacker et at. 2000) and Sulu 2000), and then terminates against the Tan-Lu(Wallis et at. 1999; Faure et at. 2001) form the fault. ..

cores of structural d\)mes, exhibit a top-NW The large-scale Wudang Shan dome (Fig. 4)sense of shear and are overlain by extensional that lies west of the UHP Hong'an-Dabie areafaults that exhumed die UHP rocks. At least in is an extensional core complex overprinted byHong'an-Dabie, the entire crystalline core of foreland folding and thrusting. Deformation in "the orogen constitutes a normal-sense shear the Wudang Shan began with an early unre-zone c.15 km thick; *e Huwan shear zone, a solved, but possibly contractional deformation,normal-sense detachment that reactivated the was followed by sub-vertical contraction andplate suture, tops the ~xtensional allochthon in sub-horizontal N -S extension during blues-Hong'an (Hacker et I at. 2000; Webb et at. chist-greenschist-facies metamorphism of the2001). Associated Triassic metamorphic core basement and basement-cover contact zone;complexes in the northern part of the SCB 40 Ar /39 Ar dating of syn- to post-kinematic horn-i.clude the Wudang Shan (Ratschbacher et at. blende and muscovite puts the extension at, orin press) and Zhangbaling-Bengbu (our unpub- prior to, 230-235 Ma. Subsequent folding andlished data); whether the Lu Shan (Lin et at. thrusting of the basement and Palaeozoic cover2000), Wugong Shan (Faure et at. 1996), sequence occurred during N-S contraction.Dongling (Grimmer et at. in press), and Jiuling The northern limit of the Triassic extensionalShan (Lin et at. 2001) basement uplifts within deformation (Fig. 4) is located at differentthe foreland SCB fold-thrust belt south and east positions along the Qinling orogen. In theof Hong'an-Dabie, which show a Triassic to Qinling mountains, the northern limit of exten-Cretaceous extensional overprint, are related to sion is the Wudang basement; the Douling unit

II

i

1_-

I li8lm'c "if' c

I 'I' f

blueschist

fold & thrust belt

Yangtzebasement

Yangtzebasement

10 km

N blueschist

Foziling GpXinyang Gp

Qinling Gp

Sujiahe Gp

blueschist

Qinling Gp

Meishan Gp Luzhenguang Gp

amphibolite

Ceno

zoic

Ta

nÐLu

Fau

lt

C retace

ous XiaotianÐMozitang Fault

quartz eclogite

quartz eclogite

Northern Orthogneiss

suture

fold & thrust belt

coesite eclogite

coesite eclogite

Yangtzebasement

Erlan-ping Gp

Northern Dabie Shan

shear bands & shear zones shear bands & shear zonesshear bands & shear zones

lineation, showing sense of motion of upper plate

Northern Hong'an

Southeastern Dabie Shan

shear bands & shear zones

SouthernHong'an

SE-NW trend

SSW trend

Central Eastern Dabie Shan

Southwestern Dabie Shan1

3

2

1

B 23

1

3

2B

1

2

3Sf

S0

S0

L

B

Eastern foreland

D287

D285

D284

D283

D287

D285

D284

D283

S1

foliation (¥) & lineation ( )

L1

S1

L1

L1

shear bands & shear zonesshear bands & shear zones

L2L1

foliation (¥) & lineation ( ) foliation (¥) & lineation ( )

foliation (¥) & lineation ( )foliation (¥) & lineation ( )foliation (¥) & lineation ( )

brittle stretch direction

115oE

30oN

Eocene sedimentsNeogene sediments

synform, antiformfault/shear zone

eclogite

coesite absentcoesite

metamorphic boundaries

Early Cretaceous volcanicsLower Cretaceous sediments

125-137 Ma syenite to tonalitepre-Cretaceous cratonal cover sequence

Figure 7: Structural overview of the Dabie-Hong'an area (after Schmid et al. 1999; Hacker et al. 2000; Ratschbacher et al. 2000; Webb et al. 2001). Areas disturbed by Cretaceous plutons are not included in the synoptic stereonets. Stereonets from eastern foreland show dominantly brittle faults: (1), (2), and (3) indicate principal stress directions; B, fold axis; S0, bedding; and Sf, foliation.

I

168 B. R. HACKER ET AL.

is non-mylonitic and lacks significant Triassic sedimentation (Huang & Opdyke 2000) ormetamorphism. In northern Hong' an, the unconfonnable deposition of coarse carbonateHuwan shear zone constitutes a lithosphere- breccias (Breitkreuz et al. 1994). Yin & Niescale reactivation of the Devonian-Triassic (1993) proposed that the transition from marinesubduction complex. In Dabie, the Huwan to continental sedimentation was diachronous:detachment cannot be mapped, as Cretaceous Early Permian in Shandong and Korea, Lower/tectonism has obliterated earlier fabrics, but the Upper : Permian south of Sulu, Lower/Middlenorthern limit of extension must be south of Triassic SE of Dabie.the Foziling and Luzhenguang units, which Nie ~t al. (1994) and Zhou & Graham (1996)have clear Yangtze craton affinity and were proposed that detritus eroded from the activeunaffected by HP metamorphism, very likely Qinling - Dabie mountain range was channeledcoinciding with the Early Cretaceous Xiaotian- westward and deposited to fonn the Songpan-Mozitang crustal-scale shear zone (Hacker et al. Ganze flysch from the Anisian through the2000; Ratschbacher et al. 2000). Norian (c. 240-2 10 Ma). Bruguier et al. (1997)

Much of the area shown in Figure 2 has found detrital zircons with U /Pb ages of 233WNW-trending folds and craton-directed thrusts and 231 Ma within the Songpan-Ganze flysch .of millimeter to kilometre scale that fonned during that m~tch the ages of zircons found in Dabiethe collision (Mattauer et al. 1985; Regional Geo- (Hacker et al. 2000).logical Survey of Henan 1989; Regional Geological Post-collisional, Jurassic, continental clasticSurvey of Shaanxi 1989; Regional Geological sedimentation on both cratons was accompaniedSurvey of Hubei 1990). On the NCB, the north- by deposition of up to 5 km of calc-alkaline, crus-directed Lu Shan thrust, placing crystalline base- tal-derived, intennediate-composition volcanicment over Palaeozoic cover, was active in the rocks: tuff, volcanogenic sandstone, and someMiddle Triassic and Late Jurassic (Huang & lava in the Late Jurassic (Regional Geological Sur-Wu 1992). Huang and Wu (1992) also identified vey of Anhui 1987; Regional Geological Survey ofa series of Mesozoic S-directed thrusts imbricating Henan J989; Regional Geological Survey of Hubeithe Sino-Korean basement, Kuanping, Qinling, 1990). Gneiss cobbles, presumably derived fromErlangping and Douling units. The fold-thrust the Dabie Mountains, first appeared in the Zhujibelt along the Lower Yangtze river began to Fonnation on the northern slope of the Dabiedevelop through NW -SE contraction in the Mountains in Middle Jurassic time (Ma 1991).Middle Triassic and continued through the Middle Jurassic sedimentary rocks in the LowerEarly Jurassic, by which time the shortening Yangtze fold-thrust belt show clear evidence ofdirection had rotated to NNE-SSW (Schmid erosion of the Dabie UHP core, including Triassic-et al. 1999). Jurassiq detrital micas with high-Si contents and

The Early Palaeozoic core of the Qinling oro- zircon grains as young as c.218 Ma (Grimmergen was reactivated during the relatively early et al. ~ press) their oldest mica ages indicate thatstages of the NCB-SCB collision by overall exhum~ion in Hong'an-Dabie might have startedtop-south imbrication during a change from at 240 t 5 Ma.NW -SE (dextral transpression) to NE-SW .shortening. Ratschbacher et al. (in press) docu- . .mented c.200-250 Ma low-grade metamorphism Plate-scale collision modeland dextral transpression along the Lo-Nan, While there is still much that we do not know,Shang-Xian and Shang-Dan faults, and N-S some key structural observations constrain theshortening within the Liuling and Douling units. exhum~tion mechanism of the UHP rocks

(Hacker et al. 2000):

Syn- to post-collisional overlap assemblage (I) Unfolding the 'Hong' an antifonn' - the

Changes in sedimentation patterns are often orogen-scale fold trending NW -SE acrossamong the best guides to collisional timing. Hpng'an-Dabie - yields aN-dippingDepositional facies up through the Permian lithospheric slab with coesite eclogite intrend E- W in the southern NCB, and NNE in the north and lower pressure rocks progress-the northern SCB (Han et al. 1989; Sun et al. ively farther south and closer to the interior1989; Wang et al. 1989; Zhang et al. 1989). of the SCB. The upper boundary of the slabAlthough collision-related (?) shortening began is: the Huwan shear zone, which encom-on the SCB in the Early to Middle Triassic, p~sses the suture between the NCB andthe major sedimentological change occurred t~ SCB, implying that it is essentially ain the Middle Triassic, which was marked plate boundary reactivated as a litho-locally by either a depositional hiatus, continental sphere-scale, nonnal-sense shear zone.

. : j J : 'C :

II

170 B. R. HACKER ET An.

two plates as the result of Late Pennian-Early ed~e of the SCB. In Dabie, it lies south ofTriassic indentation of the NCB by the SCB; th(j Luzhenguang unit. This implies thatthey rationalized that the active margin of the the Douling, Luzhenguang and other unitsNCB should have been relatively straight and (i) represent the leading edge of the SCBthat the passive margin of the SCB could have but were not subducted; (ii) were originallybeen relatively complex. Gilder et al. (1999) cri- south of the HP- UHP rocks and ended upticized this idea because of a 'lack of significant in their present position as a result of exhu-folding of Phanerozoic rocks. . . north of the Sulu mation of the HP- UHP rocks; or (iii) arebelt', and proposed instead that the older NCB part of the NCB (although of Yangtze affi-acted as a rigid indentor to deform the SCB in nity, like the Qinling unit), but are nowthe Early to Middle Jurassic - leading to the mysteriously south of the Liuling, Xinyangpalaeomagnetically recorded bending of the an(l Foziling units and escaped intrusion byLower Yangtze fold-thrust belt (Gilder et al. the Qinling arc.1999), formation of the Tan-Lu fault, and 600 (4) A weakness of the exhumation model out-of relative rotation between the NCB and SCB lined in the previous section is that we(Zhao & Coe 1987). While there is structural have not identified a sole thrust along theand thermochronological evidence of Late Cre- southern and eastern edges of Dabie- .taceous and Cenozoic strike-slip and normal Hong' an. SE-directed extrusion of thefaulting (Ratschbacher et al. 2000; e.g. Grimmer w~dge of UHP-HP rocks should haveet al. 2002), no well-documented structural data induced equivalent shortening at the tip ofdemonstrate sinistral Triassic or Jurassic motion thcr extruding wedge, but one of the charac-along the Tan-Lu fault. However, Mid-Triassic tetjistics of the Triassic/Jurassic forelandNW -SE contraction and Late Triassic-Early de~rmation east of Dabie is upright foldingJurassic N -S contraction in the eastern Dabie an afo~land (Schmi~ et al. 1999) .implies ~at if the c? bination o.f hin~erland-. and foreland-Tan-Lu fault eXIsted at that time then It would di cted thrusting WIth relatively moderatehave been sinistral. Note that the age of Triassic shprtening (Schmid et al. 1999; Grimmermetamorphism in the Qinling area is similar to et i al. in press). To explain the apparentthat in Dabie; the proposed younging and west- laqk of the mega-thrust and the distinctiveward migration of collision (e.g. Zhao & Coe stljuctural style, we can envision at least1987; Yin & Nie 1993; Zhang 1997) is not sup- thtee scenarios. (i) The leading edge ofported by extant geochronology (Hacker & th~ UHP-HP rocks forms a wedge that isWang 1995). buried beneath the cover strata of the fore-

land. This implies that the crust of the fore-.. land was detached at middle to upper

Problems and possible solutions c~stal levels and thrust northwestward onThe preceding sections have outlined a number tol the crystalline core. (ii) The UHP-HPof important problems within the Qinling - rocks were exhumed by buoyancy into!Dabie orogen. the middle/lower crust, and the overlying "! rocks were removed by extension and ero-1(1) The boundary between rocks of Sino-Kor- sil1>n. A plate rotation model proposes that

ean and Yangtze affinity appears to be a af(er initial collision in the eastern part of thesuture of Ordovician-Silurian age. This ott>gen, continued closure of the 'Songpan- "interpretation could benefit from further G~ze Sea' by subduction of oceanic litho-analysis of the tectonic histories of key sphere caused the SCB to rotate 60 0 clock-

units in the Qinling orogen. wise (required by palaeomagnetic data),1 (2) Devonian-Triassic rocks of the Liuling, pulling parts of the subducted SCB back

Xinyang, and Foziling units separate the toward the surface.NCB from the SCB. These relatively mono-tonous units thus potentially experiencedquite a varied history. Can this history beread from these rocks?

1 (3) The northern boundary of Triassic exhuma- Summarytion is generally south of the northern edge Grenvillian orogeny, involving oceanic subduc-of the SCB. In the Qinling mountains, it lies tion ~ith HP metamorphism and ophiolitesouth of the Douling unit and south of the emplacpment (Songshugou ophiolite), assembledYangtze craton cover. In Tongbai and the Ya1)gtze craton, including the Qinling micro-Hong'an it coincides with the northern contint1lit, into Rodinia. Rifting at c. 750 Ma

I '] -

SUBDUCTION, COLLISION AND ~ATION 171

separated the Qinling microcontinent from the CAO, R. ~ ZHU, S. 1995. The Dabieshan coesite-bear-Yangtze craton. Intra-oceanic arc formation ing eqlogite terrain - a neo-Archean ultra-high(Erlangping-Danfeng-Heihe) between c.490- press~ metamorphic belt. Acta Geologica Sinica,470 Ma was followed by the accretion of the 69, 2~2-242.lower Qinling unit to the intra-oceanic arc and CARSWE~, D. A., O'BRIEN, P. J., WILSON: R. N.. &

the North China Block. Oceanward (northward ZHAI~M. ~997. The~obarometIJ°fphenglte-~ngin present coordinates) subduction beneath the eclogites m the Dable. MountanIs of central China.rth L . 1. ... Jounl41 of Metamolphlc Geology, 15, 239-252.

no em ill mg urnt. lmpnnted the c.400 Ma CHAVAGNAC, V. & JAHN, B.-M. 1996. Coesite-bearingAn~ean-type mag.matlc arc o~ t~ the North eclogites from the Bixiling Complex, Dabie Moun-Chma Block. OblIque ~ubductlon Imposed the tains, China; Sm-Nd ages, geochemical character-spectacular Early Devornan left-lateral transpres- istics£d tectonic implications. Chemical Geology,sive wrench zones. A subduction signature is 133, 9-51.again evident during the mid-Carboniferous to CHAVAG AC, V., JAHN, B.-M. VILLA, I. M.,Late Pennian on the North China Block, when WHIT~HOUSE, M. & LIU, D. 2001. Mu1tichrono-the Palaeo-Tethys was subducted northward, pro- ~etriq evidence for an in. situ origin of the ultra-

" ducing the andesitic magmatism on the North hig.h-pressure metamorphic terrane of Dabieshan,fhina Bloc~. In the Late Pennian-E~ly Trias- Chinaf Journal of Geology, 109, 633-646.SIC the leadmg edge of the South China Block CHEN, D'i Wu, Y., WANG, Y.-J., ZHI: X., ~A, Q. &

was subducted to >150km and subse uentl ~~Nt J' 1998. .Age~, Nd and S~ IS.otOpl~ compo-

. . q. y sItton of the JIaozlyan gabbrolc mtruslon from

exhu.med by crustal extensIon dunng clockwIse the n rthern Dabie terrain. Scientia GeologicarotatIon of the craton. Sinic ,7,29-35.

CHEN,J., E,Z.,LIU, S.,LI,X. &FOLAND,K.A.1995.Thanks to Yongjun Yue, Stanford, for assistance with COOl~ g age of Dabie orogen, China, determinedChinese publi~ations; Shuwen Dong, Yueqiao Zhang and ?y 40 _39 ~ and fission track techniques. Science

many other Chinese colleagues for field guidance and discus- m Ch na, Senes B, 38, 749-757.sions; our colleagues J. C. Grimmer, L. Franz, R. Schmid, CHEN, ~., RAN, Y., You, Z. & SUN, M. 1992.E. Enkelmann and R. Oberhiinsli for discussions; and Whoi-rock Sm-Nd, Rb-Sr and zircon Ph-PhC. Blake, P. Robinson and C. Fletcher for useful criticism. datin of the metamorphic complex in the inte-Funded by projects Ra442/14, 19 of the Deutsche For- rior f Qinling orogenic belt, western Henan,schungsgemeinschaft and NSF grants EAR-9796119, and~eir im.plications with regard to crustalEAR-9725667 and EAR-<XXJ3568. evolu on. Chinese Journal of Geochemistry, 11,

168- 77.CHEN, .-S., You, Z.-D., Suo, S.-T., YANG, Y. &

References LI, H -M. 1996. U-Pb zircon ages of intermediateAMES, L. 1995. Geochronology and isotopic character ~u ires and d~forme~ granite~ in Dabie ~oun-

()f ultrahigh-pressure metamorphism with impli- ~~~ Ic~:~ China. Chinese Science Bulletm, 41,

cations for collision of the Sino-Korean and h'Yangtze cratons, central China. Pill thesis, ~UZ~L, ,D., JOLIVE:, L.. & CADET, J.-P. 1991: EarlyUniversity of California. lDlddf PaleozoIc mtraplate oro~en'f m the

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