6

勿 H ongzhen W ang and X uanxue M o A n o u tlin e o f th e tecto n ic ev o lu tio n o f C h in a

'Fectonicall-V C hina is com po s e d o厂three P recam brian aily bOUnded by subduction zones (here called accretional conlinenlat p la晌 rins, Sino K o，二‘，，Yangtze. Tarim , and CrUstal consum ption zones, or A Z ). 4 T erranes w ithin the Cold 7ones. I、h ese rnw ht he rc-arded as spe- possiblIN, also C athaYsia. W ith their interstitial.户/d belts, cial ca ses o f th e third i-ank . thel, 、：二re It w o rporated iogether to .1o" n part of' the T hree ranks of tectonic st a g e m ay be discerned (W ang. 1982). E ura,sian Sup ercontinent 1hrough the Indosinian R e first is inainly of a (flobal nature and denotes profound changes in the geospheres and in w orld tectonic fraines. T he second is the tra- orogen-v in the late 7)-iassic. Ili addition, there are the 山tional tectonic stage. in w hich there w ei℃川iporlant change％川tec- northern hot-det ‘，／the Indiall P hl咖 rin, the H iniala-vas tonic trarnes or patterns. T he third refers to cpoclis of intense ot-o- and the northern ，，，‘，‘、‘、叮、、，／G ondw anan 、，厅illiti(、，w hich "enic deform ation and ina.,niatic activitv. I-ive rnc,asta-(,es are recognised, w hich led to the form ation ot 、，，‘re accreted or colla t}cel m cce.%、；、·、IN, onto the I continental nuclei (c. 2.8 G a); E urasian Superconlinent in post-Indosinian iiines. N ine -) continental protoplatforins (c. 1.8 G a): tectonic doinains (a-(, w cogniw d, which al-c delim ited b-N 3 continental platform s (c. 800 M a)} 4 SUpercontinents (c. 208 M a), and intijorgeosutures called (-oil vergent critsial consum p tion 5 disinte-Iration Ofthe Supercontinent to fOrIn the present earth ：‘，，，。‘、．P ie leclollic ‘／‘velopillent，、，‘，‘、infi ve inegaslages frain e. dit，一；ng w hich w crc /0/-//le(I:./l`l.sl/v, conlinellial lilw lei（‘ 1,11c tuain leatm es and pcological events in the d ifferent tec- tonic sta,lc} of(’h ina are suirunarised in T able 1. Foi- con\ cruence ot 2.8 G ‘，）；SeCOndlY, /he p rolo-p leqtorm s （。： 1. 8 G a); discussion. " c have spccial]N included K orea in Fi}'Lrrcs I and I thinfly, the, pla功，，：，，、（‘·，SOO m a少,j Ourthiv, the E urasian N ine principal tectonic dom ains inay be reco-nised in (、h in a Silpercontinew （‘2 10 M a ), and ./ift hlY, Ille presenifi -aine (W amI, e t aL, 1990 ). T hey are front north to South (Fi}-_,urc I）： I T he A ltai-Flingan B elt (A H B ), },vhich is the southern part of the ol'(’h ina. A m on } thcs}、/Ile／，1‘，lj‘J，，，，／‘，，·，，，‘，1＊‘，，， (i t the ellel Sibeiia-M on-olia D om ain. 。，／the j；，，，11，1‘gj‘、，， o r ogeny (SOO M a ) and the superconti- 2 T he Jum - ar T ianshan B elt O f’1 3), kvhich is tire eastern part of lient八w m alioll tit the 。，，‘八，／the Intlo,sinian orogenY (210 the K azakhstan D om ain (K Z D ) 3 ]'Ile BUFCVa--JaIIIus B elt（IB B ), w hich is the SOLIthCI_u IM 11 of tlIC M a ) a re the m a m la m lil7tirks. N orth-east A sian D ornam . A ll the three dom ains are com posed 、）！Sinall M aSSH'211-OLIJ)s interconnected h\, FarIN Palaeozoic told /ones and are delim ited from each other by Early 11crcynian corivci-L,erit zones, the Erfi x-K alarricili (EK C Z ) in the w cst a nd T h e tec to n ic fra m e a n d cru sta l the H e,-,en (IIG C Z ) in the cast. 4 T he I a n in D o m a in (『I ’A D ). w h ich inc lu des the LIIIUSLI,11]V 1110 1111C developm ent of C hina platform and SUFFOUnding Palaeozoic fold helt}. 5 the Sin(）一K orea D om ain (SK D ) is SUrrOLIndCd M ainly by L arly P alaeo zoic to ld be lts w ith se }eral detached P reca m brian niassi l' s in the south. T he boundary bet" een the T A D and the SK I) is T erm inology of tectonic units confroxersial, its the Q aidarn (Q d) and the A lxa (A x ) inassit's A tecton ic u nit （）｛the first ran k, here called it tecto n ic do m ain, is a scelll to be closel} related to both dom ains. A recent study plate of com posite Structure and prolonged history of' developm ent. (W an-, T , 1994) has disco}ered an ophiolitc zone, the Eno e r I he 11OUndarie,, beovcen plaies, here callcd Cott\ CrVCI)t CFLIS(al COII- U su (IE U C Z ), \Ahich m ay be a convergent zone c1tea k cly dc li n - suniption /ones. are the rn}、川"COSLItUrcs. T he recent loose Usage of eatiruI, a southern (SK D ) and a northern (K Z D ) fautral province 山C VCF}' LISCfUl icrin 、 terraric' to c0、VCF TCCtO11iC units front com incri- durino t he Palaeozoic. T his boundary betw een the SK P and the tal platform s to sinIgle thrust m asses has caused som e confusion. III K Z D is truncated by the A ltun transcuri-crit fault in its w estern order to inake the tectonic t0FIuiI1OlOYy 11101-C SVSICInatic, w e use a segm ent (Figure I）．The Southern boundary ofthe platform in K orea is also） problem atic, because the cratonic area south （们 h e four-rank hiel-,IFCIV} 川山c hope that anihig,川tv 川ay be avoided: Irrijingang and north of the O chcon Belt belongs certainly to the ］ T ectonic doinains com posed of a continental platforin and its S K P not the Y ZP its generally believed (Y in ct：，｝．，1993 ). T his surrounding fOld bells, OF Ot a PFOL甲of' Precarnhrian niassits interpretation seem s to he supported by 山c 日identation ofthe interconnected by FaFIV Palaeozoic fold /ones 、（）、，、to forni： 、 north-c-astern part ofthe Y Z P into K orca alonp, the Ini.j ingIa riL-, m ore or less inlet-,raied w hole (W an", 198 1, 1986). 1’l ie tecton ic R iver durin" or after the Inclosinian Stage ( Figure ］）．『I he nort h - dom ains are delinnied front each other by convcroent Crustal crn houndaries ofthe T A D and the SK D are m arked h}, the cOnSLIII1pt1OII /Ones （（’2 ）that rnark- the final convergence oft he South T ianshan M azong shan convergent zone (T M C Z ) and the opposite continental inam ins. SUOILm - L.inxi convergent zone (SL.C Z ) respectively, both of 2 P latfo rm s (crato ns ) and 川（)b ile bell,,. Late Flercynian age. Evidence for collision is not m anifest角 r 3 L T n i t s w ith川a plallorni that c(）川prisc ancient continental nuclei the S l（’2 ，but biogeographic evidence seem s to be convincinIo and P] ccarnbriall basem ent of \ arious a-c-,． and those w ithin it (FIuan,_,, B . 199 1 } Li et al., 1992). m obile bell attrihutable to a single continental tract, inade tip o f 6 The Y ar qIt z e- -Q ia n-I t a n g D o m ain (Y Q D ) iI)CILIdeS the Y angItze fo ld /o n es o f vario u s }w c s w ith o r W ith O LIt in ed ian in assits. ']'he Platform in the cast and a I-roLIj) of m assil's in the w est, com p ris- to ld zo ne s a nd ru assifs o ri6 nalc fron t SU ccessivelv accreted ing the N orth Q ian-tan- (Q t), the Q arndo (Q i川 zinc] the Lin- island arcs an(] traLrucias split front the continent: they are L IS U- can,, Sim ao (I-s), w hich w ere probably parts、）！tile Y Z P that

M a rc h 浅 J u ile 1 9 () S 7

Table I Tectonic stages in th e crustal evolution Qf C hina.

E o n E ra. M egastage Stage lOrogenic epocbs and geological events M ain regim es U pheaval of Q uin(,hai-T ibet Plateau － 一 H im alayan orogenc} 30 一 K z H im alayan C lose of Y Z A Z northw ard indentat io n ol ：1 V N E India onto T ibet-Y unnafl forcland C om pression dom inant (W ) ， 卜 Intracon tm ental basins (W ) rift basins and m arginal sea s (E ) extension dom inant (E ) 6 } 一 developm ent 9 （） -t 一 Y arlshanian orogeny ︺ Form ation ot'circum -Pacific m ag m atic belt o一 N 呱 丫a n s h a n ia n In d e n ta tio n o f N E Y Z P o n to K o re a o · C lose of Q N A Z ．l t 2 （）8 ，＿ 一＿ Indosinian orogeny 门l 一尸 C ollision of T ZD . T B D ,'FA D a nd Y Q D to form C om pression dom inant d In d o sin ia n l Eurasian Supercontinent close to PAO and PTO 二 250 d O pening of T EO m ixing of G W F, C A F. A N F P A N G A E A III 2 7 0 － －一 L H ercynian orogeny － －一 一｝ Pz Separation ot'Q t and Q d from Y Z P aulacogens E x te n sio n d o m in a n t IV on platform s and fold belts Supercontinent H ercynian ！－－一 E H ercynian orogeny 300 － 4 0 ︺ 曰 fo rm atio n 一C ollision of A H B , K Z D , JB D and S K D 1 L C aledonian orogeny － P 2 1 I ConverI-ence ot'YZP and CAD collision of A x and Q m 只j，们 C a le d o n ia n ． E C alcdonian orogeny 440 O pening ot S Tianshan, 一 卜 E x te n s io n d o m in a n t O pening of Q ilian, Q inl in g 卜 80 0 寸 L Jinningian orogeny 一－ － 一 ︺ 一 一 1 （om pression dom inant ︶︵ l︵︶0 0、 III Form ation of platform s: SK P, T A P, Y Z P p 八 N G 八E A 11 ‘﹄ 知P la tfo rm Jum in 2ja n ，一 －一 E Jin n in 2ia n o ro Len v E x te n s io n d o m in a n t ︺︵1 fo rm a tio n vo rm atio n o j aU M COg en s: Y ansn a n , 入 t o n g e r d︸ Chaltai dl 丰－－ 一斗－ 一二二 L川iangian orogeny C om pression dom inant P A N G A E A I Pt, 1 F o rm at io n ot'protoplatf orm s: KD ,'FA D 11 L uliallgian } Y O D , C A D . Form ation ot'protoaulacogens 25︵︶ Protoplatform H LAU0, Liaohe, D ahongshan E x te n s io n d o m in a n t fo rm a tio n －一 一 一 ｝ 一 W utaian orogeny Arl In c re a se o f c o n tin e n ta l c ru st W u ta ia n 二 28︵︶ 州 Fupingian orogeny 招勺 Als C om pression dom inant 二 I ︺ Fupinuian C o ntin ental nu cle i: O r, JI, T h , T s, C h A g,-regation and convergence 刊J C on tine ntal n ucle i 代﹄ 32 0 (） 一； Ar, 一 fo rm atio n Protonuclei: C aozhuanl-. A nsham P riniarv c ontinen tal crust 一3 2 。〔） A r, Q ianxian ＿ 土 3 9 0 ( ） 一

H D H A D E A N Ara A rt E oarchaean Ptl N eo a rch a ean Pt3 N eop roterozoic T EO Tethyan O cean A r ,- Palaeoarchaean Ptz P alaeoproterozoic PA O P alasia n 口cean G W F G ondw anafl ora A r3 M esoarchaean M esoproterozoic PT O P alaeotethys O cean C A F C athaysian 加 ra F or others see F igure I A N F A ngaran fl ora

w ere detached and dissem inated in the L ate Palaeozoic (W ang et in the D evonian or earlier and closed in the L ate Perm ian, m ay al., 1990). The YQ D is dem arcated from the northern dom ains be represented by the Longnm cuo-Shuanglm convergent zone by the Indosinian convergent zones. the X iugou-M aqin (X M C Z ) (I-SC Z ) (L i, 1987). T he C hangning-M englian (C M C Z ) zone to in the w estern. and the Fengxian-Tongcheng (FX C Z ) in the cast- the w est of the Lancang River in w estern Y unnan represents the ern segm ent, but it is not clear how they w ere joined w ith each southern continuation of the LSC Z and is proved to have closed other in the south Q inling region. T he position of the southern at the end （们 ndosinian Stage (L iu et al., 1994). 1 hese conver- boundary of the Y Q D in northern T ibet has rem ained unclear, gent zones m ark the southern lim it of the Eurasian Superconti- but recent studies have revealed that an oceanic basin, beginning nent form ed at the end （们 ndosinian Stage (C hang et al二1992)

E p iso de s, V o l. IS, no s. I 浅 2 T E C T O N IC O U T L IN E M A P A 只 O F C H IN A

M ainly pre-Jurassic. For post- Indosinian m agm atism and basins see fig. 2

0 2 50 5 0 0 7 5 0 1a n 二 ， 1＿＿一一一一」

渭

'ITAD 逸攀炙差务竺丛婆毅狡 殊墓二少T A P'Ij TBJg 论 夕:= = m j _i:}_ S心 嵘经 气男汤 餐葬｛ O r

找 冬鲜慈 S K P ‘‘J . d .W白舀‘‘孟 荃 受 窿鬓蒜 场一岁飞蔗 心‘1 之 冬凡兮 }} 弓 ／ 芯交 Q t H h 笋 Y ZP 之之 彭 了 ︵ 之(K 要 拿 Th} 11 卜 Sb 川 资 D t 卜 T B D C h 尹 断声 主，于 Y Z P r!2 *.c 平 恢硫分了 ，、’ J n 丫二／．r 、 郊

圈 口 口 爵 图 国 国 口 曰 口 口 口 夕’ 2 le W 1 团 团 团 ／ 立 14 1 5 16 17 18 S OU 由 C b im I 卜 洲 阮 ．肠坛 妇 1 1 ～ 厂 0 3 00 1= I ‘

F igure I I Continental nuck i, 2800 T ecto n ic u n its: 一Ln Lingnan M ass扩 A Z A ccretional zones: M a (A 耐 ‘ A H B A ltai-H ingan Belt. 一H n H ainan M ass扩 2 Protoplatform s, (a) O SA Z Ondor Sum (C ) A g Arguna M assif 一S s S o u th C h in a S ea (b) A XA Z Aibihu-Xingx- 1800M a 阴匀J H g northern H inga n 一吃 M ass犷 ingxia 任刃 3 Pla咖二 and m ass价 汉翻 A加ss诱 一T B D T ib et- B u rm a D o m a in : (c) Q QA Z N orth 800 M a 口b 少 Tt Tuotuos h an M ass扩 一G d Gangdise M ass扩 Qilian-N orth Q in ling (C) 4 C a led o n id e s H m H im alaya M assif JB B Jam us-Bureya B elt. Qua－劝 (d) K W AZ W estK unlun (J) n 旧 5 H ercynides 色 Jm jam us M ass扩 一Bt B aoshan-Tengcho n g (e) K EA Z EastK unlun (j) 6 I n d o sin id e s Sn Songnen M ass if 一 M assif. （O LH A Z Longm enshan- 7 Y a n sh a n id es a n d 俐 ： X I Xilinhot M ass犷 CPD Circum -Pacif c H onghe (j) 刀im a勿 aides K Z D K azakh stan D o m ain : 一 D o m a in : 8 P e rm ia n b a sa lts (g) SC AZ Shexian-Chang- Y n Yinnin M assif 。X k X in到切i M ass犷 sh a (J) 明 9 Jinningian (R 2.3) granitic Jg JunggarM assif KdangW (h) WTAZ W upong-Yw ikai( C) zon es (j) n 〔Z C onvergentz ones: Trn 71upan--HandM a ss 犷 KdJwt五 (i) SBA Z Sibao (j) 比窗 10 Caledonian (Pz，） granitic T A D T a rim D o m a in : DtIhae－TongbAs I EK CZ E rlik-Kalarneili (H ) 0) JTA Z P nshqjIang-Teng- zones (C) TA PT arim Pla咖二 ： DOouIingMasd 2 H G CZ H eganshan (H ) tiaohe (I) I I H ercynian (Pz2) granitic T s C en tra l T u r rim 3 T M C Z S o u th T ia n s h a n 一。 r (k) B N A Z 陇 r zones (H) N u cle u s 一-M azongshan (H ) Banggo n g - N ujiang (YH ) 12 H ercynian-Indosinian (P- S w S o u th -w e s tern Qma－4 SLCZ Soulun-Linxi口刃 (1) YZAZ Yarlung Z angbo T)g raniticz ones Region 一5 E U CZ Enger Usu (H ) （Y]刃． 13 A cc retio n a l cr u sta l c o n - M j M anjya r R egion 一6 AM CZ X iugou_M aqjn 闭 sum ption zones (A Z) Q u Q uruktagh Regio n 一必 7 F TCZ Fengxian (J A nninglan; C Caledonian; 卫钻 14 C onvergentc rustalc an- A t A ltun Region -Tongcheng (1) H H ercynian; sumption zones (CZ) 8 S S C Z I I ndosinian ; YH Yansh an - B b Bayanbluk M a s sif 一． 尸 到 15 Pt2-3a ulacogens and r ifts M z M azongshan M ass犷 zgZhuanMs． Shaoxing-Shaoguan (C) lan-H im alayan) 16 Z-0 aulacogens S K D S in o -K o re a D o m a in : 9 L S C Z 一． 比 法n 17 D -T aulacogens S K P S in o -K o rea P lo t- 一 L o ngm u cuo-Shuanghu (I) SF S trike-slip faults: 18 Strike-slipfaults, m ostly form : 10 M CZ Changning- (1) A ltun; post-Indosinian. O r O rd o s N u c le u s 一M eng lian (I). (11) Tanlu.

M a rch ＆ J un e 199 5 7 T he C athaNsian D om ain (C-11)), lorm ed ol'Precarnbrian m assits that they originated Separately and m eie latcr zw giegated togeth-cr to Inco）rporated in the Early Palaeozoic. and thus com parable w ith form the protoplatform s the K Z D , w its probably a part of the South-east A sian palaeo- continents. J lie relation betw een the Y Z P and the C 1 D has lon g Protoplatform s been d iscussed (G uo et al．1989 ). It seem s doubtless that a w id,.Sprcad Prccam brian basem ent existed in south C hina to t he T h e N e oarch acan (2.8 -2..5 G a , A t几1) it) north （二h ina includes fire south ofthe Y Z P in Proterozoic tim e, w hich becam e som ew hat W utai. Luliang 'and Jia112xian groups rit Shanxi and pos,,ibl} the dissociated and collided w ith the Y Z P in the Early Palaeozoic D am azi G roup in eastern H ebei, lorm ing the 、、）called L p,irch·iean interval on the S K P . It is ab sen t in rn anv o1he r are as. Ihk-,,c ro ck,} 丁lie conver-ent zone betw een the Y ZP and the C T D is tenta- li%,,Iv draw n fi-om Shaoxing 10 ShaO."Llarl (SSC Z ). It continue s represent greensione belt,, probably of exionsional orik2m , all(J %%crc l'urthe r to the so uth . intensely tolded b,, the W titaian orogeny and nietam orphi"til (2-5 8 T he 'l’i bet--BLI；一，iia D om ain (T B D ). occupying the northern bor- G a). w hich rnark}}d a conspicuous cratonisation of no）rth C hina. 'I he der part,, ol'the Indian Plaf orm . consists of the H im alayas M as - succeedine Paiaeoprotcrozoic (PtJ）rock.,; com prise tw o tcctono-w d- im entary types. it rift-geosyncline type （M i lanovsky, 1985) or pi oro - 、，｝一‘H in ), tile G anudise Nl i,;sil-(G d) and the southern Q iangtarn, aulacogen t}pe （W ang and Q iao, [()84) and a seiri，一‘table m arine area, w hich are dem arcated by the Y arlung Z angbo (Y Z A Z ) and basin type.T he first is represented by the H UtU0 G rOUP and its equiv- B anoco n-2- M ljiang- (B N A Z ) ophiolite zones. T he Indosm ian alents, containing clastics and argillites w ith inctaba}ic rock,, o t M aSsif`}eerns to be related to both the Y Q D and C 'f D , and the bim odal pattern. 'rhe second is represented by the Songskan G roup South C hin a Sea M assif(Ss) m ay bear a closer relationship w it h containin- w ell-sorted clastics and carbonates. Both w ere folded and 八LISt r}lI i a- m etam orphosed during the Lulian-ian oi-o,,cnv O kang and 0 Ia O. 。 T he C ircurn一Pacific D om ain (C PD ), w hich includes the X inpkat 1984 ). C ontem poraneous locks in Liaodong of north-e}ist C hina 'M assit（X k } and the Y anbian area of north-east C hina. both include M g carbom nes and tUrbidites. som etim es atiainint, 111,12C carne probably from the w estern P roto-Paci tic Lind becam e c o l - thicknesses. I he 'X 1.0aiall and [AiliallgiOn oro genies。lused the sep - laged to east A si：曰n the Indosm ian and later stages. arated n uc lei in n orth (’h in a to coa lesce a nd le d to th e fi na l form atio n of' the SK protoplalforin. T he southern houndjr,, of the protoplat- form w its alorn-, the southern border of the Q n-ilinp, i.ofle. -,N hich kN a, C h in a in P resin ia n tim e s 一 th e probablv split and shifted 10 the South in the M esoproterozoic (Pi-) form ation of continental nuclei, In northern T arnri, T he Pi 1 H indu,,.,, G roup i,, variable in lithol － ogy and is in som e places Sti-01121V tOW C(I itud m etam orphosed protoplatform s and platform s partly to arnphiholite lacies. C ontem poraneous locks in A ltuii and w est K unlun show even strorw er tricianiorphisin．T his represent,, the L uliangian oro-criv w hich led to the form ation of- the l arin-i proto- platform includine, the Y ining,（Y n) and B avirblUk (f3b) inassit's in C o n tin en ta l n u c lei ce ntral and so uili If J a nsha n. It ，％［（）be no ted that th e N1c s(）一and N eo - proterozoic sequences and lithologN in northern Tarim , A lxa C ontinental nuclei o[considerable size form ed prior to 2.8 G a an(] Q ajdarn and north C hina are all sim ilar to cach other, and the Sino- occur in tile sim ）一K orea, the Y angtze and possibly the -farim plat- form },. -1 he oldest rocks are in the 川iao N ucleus 0 1) in eastern H ebei K orea and 'farim protoplafornis m av ha-Nc been ilien iin ci-corinecled or a t least c lo se to Lcilict and Liaonnw , },vherc detrital zircon, w ith a U --Pb age ot'over 3.0 G a, A ncient crystalline b a se m ent in the Y ang-t/c region is confined w a., obtained from the H uan2lbaiYU Q uartzite, Jixian, and ancient to the. north of' the ．l iarignan Region (.111). but the D ahie一- T ongbai grarittic continental crust, 3.8 G a old. w as reported from A nshan. M assit (D I) w as probably it part of')ra notze in Pit tim e. T he D alionu - Liaoning （LJU 以A ., 1992-, C hcng, 1994). both of E oarchaen (A n ） shan G roup in central Y unnan is it sodic alkah volcanic series and age (T able ｛）N ear A nshan. banded ironstone form ations (B IF ) of m ay represent a protoaulacogen form ed oil thin sialic CLUSI on the A 1,101nall type W ere f`OUnd LIFICOnforniably overlying granites 2.8 G a inner side ofthe K anqdian R egion (K d). T he Sibao G roup, form erly ill age. T he H chUai N ucleus (H h) contains the Taishan G roup repre- thought to be Pt, but recently pro ved to be Pt, in age. m arks the sentim , a ,rani tc- },reens tone terrain, and the T aihua N ucleus (1 h) SOUth-eastern boundary of' the Y angtze protoplatforni, although its contain,; both the D cngfen,, grani te-green stone ten ain and the J ai- inelab asic co ntent d eno te s a cru st o f transitio nal n atu re . In the （、11) hLia tronciliieiiiite-tonalite-2i-anodiorite (TT G )-type hi-h grade ter- in SOLIth-east C hina (H -ure ］）、isotopic ages over 2.5 G a are kno,,kn rain. Both of- them contain rocks older than 2.8 G a. T he m ajor part of front Z hcjjan.- and Fujian, and PI，basem ent rocks f B adu and J;anou the O rdos N ucleus (O t）subsided, but aerom a m etic data denote its groups) reachin,-, arnphiho lite tacies aie w ell knov ri (D ong cl al_ ancient nature, and a latitudinal M esoarchaean (A r3) 1-ranulite helt is 1996), indicatin}(, the presence of an extensive ancient bascm -cirt at distributcd all along the Y firshan R ange in the north. A nother that tim e. It is probable that at 山e end of Pti （1.8 G al the proto- nucleus in-w, be reco,nu sed in southern A Ixa. w here the basem ent plaform s form ed in (Au na through the I-Lifiangian orogeny bad it contains loranulftes of' presum ably M esoarchaean age. T hese nuclei w ider extent than the present platform s. In faet, around ］.9- 1 .8 G a. form ed the m ain grain of the ancient tram e of north C hina and later a pronounced increase ol'continentai crust and a w idespread craton- coalesced to form the Sm o-K orea protoplatform (C heng et al., isation m ay have occurred, in C hina and probably all over the w orld. 1984). and the extensive protoplatform s that w ere form ed m ay have joined T h e C entral I arnu N ucleus （rs) occupies a central position in w ith each other to form Pangaea （PanL,aca I in T able I）．T his is the I’a rim Basin. A n isotopic age over 2.8 G a w as recently reported partly the reason w hy w e prefer to put the low er boundary of M eso- from A rchaean rocks in Q Uruktagh. O n the Y angtze Platform the proterozoic at 1.9 instead of 1.6 G a (W an-. 1986). oldest rock is the K ongling TT G gneiss in the G orges region w hich has an a(}e ot'2.8 G a. T his represents the upw arped border part of the P latform s C entral Sichuan N ucleus (SC). the M esoarchaean agtre of w hich is suggested by the presence. in the Sanjiang area in south-eastern t一he Pt, and Pt, rocks constitute paiacover strata on a consolidated G UIZI10U, of detrital zircon, aged 2.8 G a and evidently of northern Sino-K orea protoplattorin . T he Pt, （1.8- 1 Cla) includes the C hang- provenance. A s indicated by the pronounced geochem ical differ- chengian （1.8- 1.4 G a) and Jixianian （1.4 一I．（）G al) svstem s. T he foi ences between the Tailm a and Kongling rocks (Zhang et al., 1994) m er com prises in the basal part aulacogen fluviatile deposits 角I- that constitute respectively the nuclei T h in the S K P and Sc in the low ed by clastics and carbonates containing som e K -rich volcanics Y ZP. these tw o platform s w ere probably rather far apart from each in the Y anshan reLion. w hile the latter includes carbonates of' w ide other in the A rchaean. O n the w hole, it seerris reasonable to assum e transgression in the low er and of' lim ited m arine basin in the uppor

肠，isode.v, Vol. /8 ，，‘）、．I & -1 /0

part (Sun et L u, 1990). T he low er part of Pt3 tQ I，lgbalkou‘In Crust resulting from this rifting, is indicated by the presence of Pi-4 1000--800 M a) represents true co）ver strata, but local deep trough fill- ophiolites near A ilaoshan (L H A Z ) in the H onge V alley on the w est- in- reaching huge thicknesses Occurs in L iaoning Province. A t the ern m argin ofthe Y Z P. M eanw hile, in the eastern part of the K ang- close of the Q ingbaikouan Period. general uplifting, coeval w ith the than B elt, a deep aulacogen developed receiving %,cry thick volcano- Jinningian orogIeny, occurred and the S in(）一K orea P latform w as sedituentaries, the K unyang and Y anbian groups of Pt} age. T hese finally consolidated. Subsiding belts receiving m arine deposits of w ere intensely folded. at记granites w ere extensively em placed as a Sinjan (Younoer Pti) age still lingered in the eastern part of the SK P. result ofthe Jinningian oro geny. A long the south-eastern m argin of Both the southern and the northern m argins of the Sm o-K orea the Y Z P is the Jian"In a n R egion (Jn), w hich com prises a P1-,：arc and protoplatform underw ent a com plicated history in Pt, and Pt3 tim es basin system that indicates a general eastw ard grow th of’ continental T he X ionuer aulacogen, w ith calc-alkafi bim odal volcanics, m ay crust (SC A Z and S BA Z ). T he north-eastern segm ent of the Jn is have been the interior failed arm of' an tripartite rifting system com plicated and Palaeozoic rocks w ere involved in a inetarnorphic brought about by the southw ard splitting and shifting of一 the Q m ling belt 2ellerally designated as Ptl-一3 . N evertheless. there call be no zone. T he resultant K uanping m argIinal tuarine basin received sedi- doubt about tire Proterozoic Southern h0Llndarv of the plattorni-：、、 m erits from both the northern passive m argin and the southern Q in- Jinnin-ian -ranites are extensively developed along the southern lm g island chain. It W as 山e Jinningian orogeny that brought about border ofthe Y Z P frorn southe rn A DhLJi 10 W estern J11an-l"Xi. the closure of the K Lianping basin and the northern accretion of the The ("I'D , as pointed out previously. is com parable w i th the Q inlina zone through an arc-continent collision (Z hanIo ci a).. 1994 ). K Z D , but, unlike the latter, 110 L}ItC PrOle l-OZOiC and E arly P alacoioic T he northern m argin of、 the SK I' w as characterised by developm ent ophiolite zones have thus Jar been found. Pt,_-} m etascclinrents and ol'the m ainly Pt-) m arginal aulacogcjls, the inner C hartai helt and the nretavolcanics overlyino the A r- Ptj basem ent are Aidespread, but outer B aiyun--O bo belt. D issem inated nlinor m assit's recently desig- carbonates rarely occur. T he Pt-)-3 B aoban O rOUP W dS recently found nated in N ei M ongol such as X ilinhot (X I）m ay represent border oil the H ainan M assif (H n) and in central and w estern G uan-dono fragm ents that split oft' and m oved to the north in the N eoproteio- Jinnin-jan _,,rainics are reported front northern Z heijang, and are cvj- z O ic dently the southern counterpart（们 he Jinnin6 an collision -raniles T he northern m ai- in of the Tarin) proloplatform has had a corn- al0flg [Ile SOLUIM -11 bordcr of Y Z P. It scerns that during the Protf O- plicated history. In the w estern scI-inent, the Y n M assif w hich w as zoic, the Y Z P and C T D w ere prohah1v separated I rout each other. then still a part of' the protoplatforni, nu ght have rifted aw ay and althouoh they becam e partly connected at then- castern parts through reaccreted to thc T A P again in the JinningIian. as is m anifested by file collision at tire end ofthe Jinnirw ian Sta-e. presence of* a blue schist 70(）一900 M a in a-Ie in tile A ksu G roup in Suniniarisino, at the close of the Juinin - ia n Staue (800 M a), the northern I arim (X iao ct al.. 1992). In the southern part ofeast 'I ian- S K P w,as probably 1110re CXteDSjVC than now ada}s both to the not Ill shan, the Pt2 K aw abUlak G roup m ay have been deposited oil the 之a11n1‘d1 5S（o）tultlhl．. 之atlnld the 1n1Oorthern Iin之a生【i-g,_in w as ruainl} of、 a passi\e air(] northern passive contincntal m argin Facing all ancient ocean to the rifted njitil℃ 'Vhc Q d, Q c and Lx nrassifs in the SOLUll-" CSt " Cie Still north. A long the northern border of 山ec ’'1I、'A P a, troug卜like hasin connected }O th the A lxa rc-ion in the north, hLll the southein illar-ill developed receiving very thick, Pt2 and H 3 clastics and carbonates 、）！Q d w as probably faced h} an ancient occan. T he Q inlino arc /one alm ost devoid of volcanics, upon w hich w as Superim posed the Sin- had rcaccrcicd to the SK P thrOUIgh all arc --continent collision. T o the ian Q UrUklagh aUlUCOgC1l hcaring volcano-sedinicntarie,, and east of the T anlu strike slip faull, the b0LllldM_y beiv cen the S K IP and glacigene deposits. In the T ieklik region north of w es( K unh-111, the Y ZP in Shandono is m arked bv the JintrinLman vranitc zone. T hev Pi, and Pt3 strata are of a stable cover type. w hich m arked the south- probably collided w ith each other along thiS part（们 lie boundary. ern lim it ol'the plallorni. T he,, scein to overlic the crystalline base- 'I'lic J A P " as still co nnec ted w ith Y n in the no rth , bu t there w ere m ent K arakash O rOidp, although the contact Fel,111011 has not been anc ient oc ean s b oth to no rth o f K aW abU la k a nd to the So uth o f K u n- found. In w est K LM ILID, iflon-I the southern border of ille TA P, Pt3 [Lill. E lle relationship bet\A,,een the SK I) and 尸V A P is difficult to judge. granites （们 -type are often ruet w ith, probably along the northern side of、 the W est K unlun A ccretional / one ‘K W A / )（｝｝一Jlnn理ngi之更fl T he sim ilarity of Pt-_3 siratigraphical sequences W OLlid Put thCul age. Pli granites arc also know n in cast K unlun to the south of the to,m hcr, but im m ediately after the .1inninpian orogcriv. in the Early Q ajdam M assifU jan- ct al., 1992), probably related to the cast K un- Sinian. they seerned to have separated froni each W her, as nijni- lun A ccretional Zone （K E A Z ) (F igure I）．It seem s that there w as a fested by paiaconragnetic data and by the different stratigraphical no rth w ard subd u ction o f ocea nic crust o n th e so uthern side of the dcveloprilent in the Sinian, O n the " hole, at the close ot the )in- TA P and SK P durinI- th e .1inningIian Stage. ninI-i a n Stag-e, the m ain platform s in C hina seerned not to he far apart In the Sherion-iia region. ne a r th e norhern m argin ofthe Y Z P from each other. T his is supported by palacornagnetic stu山CS thick clastics and carbonates Of Pt-1 3 age are developed. T hese rep- recently carried out by Z han,, et al.（1985 and afterw ards), and ,in resent aulocogen-type sedim ents ind icating a rilted origin. T he invesli,ation ofthe global palaeornagiletic data secrus to favour the D abie-longbai M assjl'(f)t) of A i-4-Pti a-c and the f)oulin(, M assif idea ofa Pangaea around 800-900 M a (Parigaea 11 in T able I）in the (D I) of Ptj age w ere probably rifted aw ay from the Y angtze in Pt,, E arly N eoproterozoic. and the W udang volcano-sedirnentaries' and its equivalents to the cast m ay represent the rocks form ed in the rifted trougIhs. T o the w est, the Precam brian FupirnI, M assif (Fp) m ay have been split front C h in a from th e S in ian to th e T riassic- the H annan region, the present northern border of the Y Z P. The the form ation of supercontinents new ly generated oceanic crust w its subducted Southw ard under the Y ZP, and a clear subduction sequence of geochem ically different granite zones has been observed in the X ixianlo area (G ao et al二 T his inegastage contains three tectonic stage,,, the C aledonian, the 1990). T his cvidentIv resulted from the Jinningian orogcny, after H crcynian and the Indosinian. the latter tw o usual]) not separable w hich the northern in ar-in （们he Y Z P becam e passiNe. A long the front each other, especially in south C hina. In the beginning 〔）！一the w estern m ar.-in of the Y Z P. f’rom L ongm erishan to H ong he. the Sinian, the principal piatf'orm s of' C hina began to drift aw ay from N eoarchaean K an-ding G ioup and its C(f-fivalents, corriposed of cacti other, and in the C am brian and O rdovician the tectonic re(Inm e am phibolites and ringruatised gneiss of TI’G type, and the Pt, w as essentially extensional. T he close of一 the 〔alcdorrian Stage D abongshan G roup of inetavolcartics and inctasedinients m ake up brou,,ht about the reaccretion of the Q d to the S K P and the collision the w estern m argin of the present platform . Further to the w est, the o f- th e Y Z P w ith th e C T D , bu t other interco ntin ental oce anic b asin s Lingcang Sirno M assif (I,s), hearing “basem ent form ed of the Lan- still rem ained. D uring the I-ate H ercynian and Indosim an orogenjes cang G roup of Pt 1-2 age. w as probably rifted aw ay from the w estern the plati-orrus and m assit's w ere assem bled togethe，一to form the (present orientation) m argin of the Y Z inother com inei们 it P1, tim e. Eurasian Supercontinent, w hich constituted the northern part of Pan- T he Subsequent eastw ard subduction of the new ly form ed oceanic Pa e a III crable I）．

材 ell-c h & 了W IC ／9 9 5 j l

T he C aledonian Stage ern and central part ot tire platform . Stable m arine sedim ents pre- vailcd up to inid-Perinian tim e, w hen paralic and terrestrial deposits T he Sino-K orcan Platform w as m ostly cxposed in the E irly Sinian. only becam e predom inant. ]'he SK P had a passive northern m argin in the the eastern pail being subsided. The Late Sm ian glacigene deposits are D evonian, though D evonian deposits arc absent inside the platform . distributed alonaI the southern and w estern border of the platform , and A ir oc eanic basin e xisted further to the no rth, w hich w as co nsum ed are also know n in northern Q d and northern T A P, indicating that these in the Early C arboniferous. I his is m anifested by the H egenshan m assil's w ere not仙·from each other at that tim e. Q d began to split aw ay ophiolite zone （H G C Z ), w hich m arks continental collision betw een from the SK P in the C arribrian, first form ing the north Q ilian and then. in the S K ID and the Sibe ria-M ongolia D om ain for the first tim e. In the the O rdovician, the south Q ilian oceanic basins. O phiolite and ophiolitic m eantim e. sea w ays and m arine basins still existed in the nielange zones are w ell developed in north Q ilian. T he oceanic basins Soluon-L inxi belt, oil the evidence of Pcrnuan lurbidites and possi- beI,,an to shrink in the Late O rdovician and closed in the Late Silurian b1c ophiolites, reported in the L inxi area near the SLC Z (W ang ct al二 E arly Palaeozoic arc type volcanism is frequent and granites of both SUb- 199 1）．Strong Support for this view com es from biogeographic evi- duction and collision type are know n (in both sides ofthe A ccretional dence. N ot onlv w ere the Early Perm ian cool-w arin w ater farm a and Z one (Q Q A Z ) from northern Q aidam in the south to southern A lxa in the the Tethyan w arin w ater tauna dem arcated by this belt, but the line north. T he north Q ilian C alcdonides continue south- castw ards to north betw een C athaysian and A ngIaran floia nray also he traced from Q irihng, w here the oceanic basin w as subducted under the SK P after the D aofingshan in tire w est to the Y anhian area in the east. T he barrier O rdovician (Zhang et al., 1988). C ontinental collision does not seem to disappeared in I-ate Perm ian, w hen the palaocontinents finally col- have occurred, as only a few subduction-type C aledonian granites arc lidcd. B oth the carly H crcynian H G C Z and the late H ercynian SLC Z found in north Q infing, and south Q infing regions. The com plicated and are significant, as the form er m arks the boundary betw een the A H B rifted passive m arIgin oft he Y Z P, had m ostly rem ained. a nd J13B and the latter b etw een th e JB B and S K ID . T he SK P is b o r d ered in the north by a narrow strip of' C alc- In northern X iiiiiang-1, c ollision betw een A lt a i and Junggar d on id es w h ich co ntain s C arribro -O rd o vician island arc vo lca no-sed- occurred alomI, the E KC Z (1-i el al., 1982). T he convergent zone here irnentariCS. Unconforinably overlain by Late Silurian clastics and has a com plicated history and several en }(五elm i ophiolite zone、一the carbonates near the O ndur Sum accretional zone (U A A Z ) (T ang et A lm antai and the K alaincili, have been found (X iao 以 al., 1992) al二1993). T he south T ianshan oceanic trough to the north of the The m erging of F Uanicrican, A rigaran and C athaysian floras in T A P w as probably initiated in the O rd ovician and persisted into the northern X injiang in the Late Perm ian denotes the final asseniblim , L ate Palaeozoic. Partial subduction m ay have occurred in Silurian- of the A H B , K ZD and 'TA D into the E urasian Supercontinent in the D evonian tim e, w hich had caused the uplift ofthc T A P after its rift- L ate H crcynian. imI, a n d subsidence in the C am brian and O rdovician, especialiv- in A nia.lor pa r t （们 he T A P Underw ent L甲lift after the Silurian. the M anjyar region (M g) (Figure I）．T he narrow C、a ledonicles belt D evonian clastic lerre.,,trial deposits w ere w idespread on the plat- borderim , the Ju[i,L,, I,a r a nd other inassifs in northern X ir}jian-I is char- forin and rifting and subsidence again prevailed in the C arboni丘r- acteristic o f the K Z D . A s th e S ilu ria n T uvac li a faun a w as fou nd bo th ous. A m arginal aUlacogen, of ( arboniferOUs age, w as developed in the A H B of the Siberia-M om l0lian D om ain and in e}lSteru JU111- along the K udi zone in north K unlun and a strongly Subsiding belt gar of the K azachstan D om ain, these tw o dom ains w ere probably not w as fortned in the SOLIth-W eStCrn part of the platform (H -ure I）．The separated by w ide oceans in the Early Palaeozoic. co llisio n be tw e en th e SO LIth -c astern b o rd er o f the T A P and the w est- A s noted previously. the Jinflingian orogeny bro ug h t about a partial ern border of、 the SK D , including Q d in the south and A Ixa in the collision of the Y ZP and the C TD in w estern Zheiiang and northern north, (Figure I），probably occurred alo w , the A ltun U-MISCUrrent Jianoxi. Pan (in Liu et al., 1993) thinks that these tw o m assils collided all fault and along the FU C Z , also in the L ate H ercynian. In short, at the along their m argins, but later, oceanic troughs and basins tonned end ofthe H ercynian Stage, the oceanic basins betw een the northern betw een them by rifting in the Sinian, probably the result of strike slip continental IM ISSCS, usually collectively know n as the Palasian faultin-. H e has draw n the boundary betw een the Y Z P and the U I D O cean, had all disappeared, and the m ain oceanic bjsins in the South along the Q infang residual seaw ay to the w est of the Y unkai M assif w ere part of Palaeotethys. (Y k). W e, on the contrary. have interpreted the Y k and the W - (via A t the beginium ,（）！t h e D evonian. the northern m arginal m as- Y ingyang-uan) as m arking the eastern m argin ofthe Y ZP from the pres- sits of the south Q inling region w ere quite near to the southern bor- ence of Sinian arc-type volcano-sedirricritaries. and Low er Palaeozoic der of the SK P. and the m arine basins in south Q inling actually continental slope sedim ents found to the east of that line. I’h is places the received sedim ents partly front the north. T he seas w ere shallow and convergent zone (SSC Z ) east of the Y k (Figure 1). In fact, the central narrow , as exactly the sam e D evonian fi sh rem ains w ere found in H unan-eastern G uangxi region w as a back-arc basin w ith a transitional Y unnan and N ingxia, north ofthe G ansu C orridor. T he ［ate Palaeo- basem ent crust, and w as not strongly folded in the C aledonian orogerry. zoic seaw ays on both sides ofthe northern m arginal m assit's ofsouth The m ain belt of strong C aledonian m aginatism and m etam orphism run,, Q inling w ere opened to the w ide ocean in w est Q infi ng, and from W uyishan south-w estw afds to northern G uangdong. The H ainan extended eastw ards along the southern border of the S K P (W arigg M assif(H n) w as a constituent part of the C TD , but the South C hina Sea 1981 ), as proved by the recent discovery of Early I riassic open sea M assif(Ss) w ith an A ustralian affinity ofC am brian trilobites, w as at that radio larians to the north of the T onghai M assif (T b). I’h is Late Pat- tim e still彻一aw ay to the south. 'I he C aledonian fold zone in northern aeozoic and T riassic m arine trough along the southern border ofthe V ietnam m ay indicate a closer relationship betw een the Indosinia M as- SK P w as finally closed during the Indosinian orogeny (F IC Z ) sif and the Y ZP, but that betw een the Indosim a and the South C hina Sea (W ang, 1986). m assifs rem ains unclear. G uo et al. (1989) and C hen et al.（1992) have A t the end o f S i lurian, the Y Z P and the C T D had united in south both discussed the plate tectonics ofs outh China in the Early Palaeozoic. C hina, and the only residual seaw ay w as along the Q infang belt, T he Early Palaeozoic tectonic pattern in the Tibet Y unnanD ornain w hich w as probably connected w ith the south-w estern oceans. In (T Y D ) is obscure. A n analysis of the O rdovician and Silurian biogeog- D evonian tim e, extensional conditions prevailed in the m argVinal raphy seem s to indicate that the separated iriassifs, (H m , G d, B t) consti- parts of the Y Z P, especially in its w estern and south-eastern m ar- toned an integrated w hole and show close afinities w ith the Y Z P, but the ginal tracts. The northern Q jangtang and Tangla m assit's began to O rdovician faunas show also sim ilarities w ith those of the SK P. They depart from the Y Z P, and riffi ng f’requently occurred to form w ere oil the w hole of A ustralian (G ondw anan) affinities (Y in ed., 1994) Im icroaulacogens' in the H unan- G uizhou-G uangxi region. Exten- sional processes w ere strengthened by Perm ian tim e, leading to pro- T he H ercynian and In dosinian stages fuse eruption of' Perm ian and T riassic continental and subm arine basalts and to the form ation of' rift - and arc-type volcanism in the In the Late P alaeozoic, a m ajor part of the SK P r em ained exposed hin ited oceanic basins in the triangular region of' Songpan-6 arze from the tim e ofits upheaval in the m id-O rdovician, until the M iddle (H uang and C hen, 1987} ('ban- et al二1992). To the w est of the Jin- C arboniferous, w hen epicontincnial seas began to inundate the east- sha.jiang, oceanic basins ot'considerable w idth existed on the castem

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r . 21 El . . E 0 2 r 0 i 1 2 3 4 5 6 o f to N F-I P -7.1 P 71 M 9 F -7- m r i v ' . 1 0 o } o D 7 8 9 10 11 12 o o o o o f P R B 0 F771 F7,1 0 1 2 !] ZI 2 G S o u th C h in e I S ea Islan d s 1 3 14 15 16 1 7 1 8 o } L -11011-

F ig u re 2 1 Continentalp latform s and m assifs JQ B J iuquan B asin 2 Tri assic-C retaceous basins/foreland basins O R B O rd os B a sin SC B S ich u a n B a sin 3 E arly Cretaceous (including Late Jurassic) basin group 4 C retaceo u s ba sin s S L B S on g liao B a sin B H B B eh aiw a n B asin 5 L a te C retaceo u s- P a la eog en e b asins 6 P ala eogene-Q uaternary basins JH B J ian g h a n B asin 7 Indosinian granites (I-type/S-typ e) Y G B Y in g eh ai B asin 8 E arly Yanshanian granites (I-ty p e/S-ty pe) S Y B S o u th Y ello w S ea B asin 9 Late Yanshanian granites (I-typ e/S-ty p e) E C B E ast C h in a S ea B a sin 10 Late Yanshanian-H im alayan gran ites (I-ty pe/S-typ e) P R B P ea rl B a sin 11 In d osin ian ca lc-a lk alin e volcan ic rock s O K B O kin a w a B a sin . 12 Yanshanian calc-alkaline volcanic rocks (andesite-dom i- C Z C on vergentZ ones (op en circles): nant/rhyolite-dom inant) 1 X M C Z X iug o u - M a q in 13 Y a nsh a n ia n h ig h -K vo lca n ic ro cks 2 F T C Z F en gx ia n - T o ng c h eng 14 C enozoic volcanic rocks (high-K ty pe basalts) 3 L S C Z L on gm u cu o- S h u a ng h u 15 con verg en t zon esla ccretio n al zon es 4 C M C Z C ha n g n in g -M eng lia n . 16 th ru sts a n d n ap p es 17 stri ke-slip f aults A Z A ccretional Zones (black circles): 18 faults in g eneral. 1 2 J TA Z Jinshajiang-Tengtiaohe JG B J u ng ga r B asin 3 B N A Z B angong-N ujiang Y L B Y ili B a sin YZ A Z Ya rlu n g Z a n g bo . T M B T a ri m B a s in T H B T u rp an - H a m i B a sin SF Stri ke-slip f aults: Q D B Q aidam B asin (I) A TSF A ltun; (II) TL SF Tanlu; (III) H H SF H ong he.

M a rch & Ju ne 19 95 13

side of the Q rn and L s m assits. T he closure 、们 hese oceanic basins Y anshanian crust-derived m uscovite-bearing granites in the Low er and the form ation of Inclosim an convergent zones (L SC Z and Y angtze region (D eng et al., 1992), and by the presence of dia- C M C Z ) to the south and w est of Q t, Q nri and Ls, m arked the north- niond/coesite-bearing ultra-high pressure m etarnorphic rock belt川 w ard accretion of these m assifs and the southern boundary of the the D abic re-ion. T he tim e of high pressure m etam orphism is con- new ly form ed E urasian Supercontinent. troversial, but it w as probably fornied by the rapid Indosinian lithos- A s m entioned previously, the m a}jo r g e osuture dem arcating the pheric convergence, and w as brought to the surf一ace by the Y anshan- E urasian Supercontinent in the north and the T ibet-B urm a D om ain ian uplift on the collapse of the orogenic belt. T he A -type granites in in the south has long been controversial. E arly Perm ian fillites and Jilin-H eilong.iiang region of north-east C hina probably had the sam e cold w ater faunas indicating a G ondw anan origin are not found north origin througIh the Indosm ian orogeny follow ed by collapse of the of L ongm ucuo and Shuanghu. T ypical V is6an faunas occur to the orogenic belt. north of G erze and a south C athaysian flora of Late Perm ian age is In east C h i n a , the Y anshanian Stage w as characterised by intra- found in Shuanghu. T here seem s little doubt about this m ain bound- continental collision and further w elding of the m ain platform s and ary, although the oceanic basin to the south of it m ay not have been ruassifs. T hrust zones have ]om , been know n from the Y anshan so w ide as previously thought (W ang, 1986 ). It m ay be noted in this region w ithin the SK P, and m ore extensive thrust and nappe zones context that. from a biogeographical and palaeornagnetic view point have recently been discovered to the north of the Larg shan R ange in Palaeotethys, betw een the northern and the southern continents, N ei M ongol.T he giant T anlu transcurrent zone (Figure ］），the im bri- seem s not to have been w ide enough for the palaeocontinents to be ca tion slices form ed o f P ro te rozo ic strata in northern A n hu i a nd th e globally reconstructed. The presence of a C athaysian flora in south- various thrust zones fo und in the low er Y angtze and central H unan. w estern U SA is also difi cult to reconcile w ith our present know l- w ere probably all form ed at this tim e. 'The Y anshanian volcanic edge of palaeophytogeography and palaeocontinent reconstr-uction. rocks and granitic intrusives in east C hina w ere m ainly form ed by intracofltinental convergence at记 subduction} probably resulting fro m th e d istant, in la nd infl ue nce of su hd uctio n of th e K ola-P acifi c C hina in post-Indosinian tim es 一 Plate beneath the Eurasian Supercontinent. 'They are distributed in three belts striking in a N E-SW direction as follow s: intracontinental developm ent I T he H m (,ari-Y ariliao m agm atic belt consists m ainly of J i-K i （145- 11（）M a) terrestrial volcanic rocks and gIranites of both S - and 1-type. 130-95 M a in age, in the D axingan l ing region, and T h e tecto n ic fra m ew o rk a t th e close o f th e （们 -type. 138 M a in age, in the Y anliao region. V olcanic rocks range from calc-alkaline basalt-andesite association to intracon- Indosinian Stage tinental extensional haw aiite-trachyte-peralkaline rhyolite asso- T he close of the Indosm ian Sta-e m arks an im portant turning point ciation. T his change in rock association w as coeval w ith the in the tecton ic ev olutio n o f C hina an d led to th e fi n al form ation o f the conversion from com pressional to extensional conditions in th e Eurasian Supercontinent (C hano et al二 1988). T he closure of regional stress field of east C hm a, after w hich the rift basins of Palaeolethys in the L ate T riassic had left scveral convergent and north C hina w ere extensively developed (M a et al., 1987) accretional crustal consum ption zones m arked by ophiolite and ophi- 2 T he C harigbai- Lo, er Y ari-tze m aornatic belt stretchina froin olitic m elanoe zones of Inclosinian aoe. T he convergent zones Zhangguangcailing in the north to N anling in the south m ainly include the X iugou-M aqin (X M C Z ), the Fengxian-T onacheng consists of 1, to K , （169-85 M at high-potassiUM calc-alkaline (FT C Z ) and its eastw ard extension in southern Shandong. the L ong- andesite-dacile-rhyolitc and stioshonite-inugearite-trachyte vol - m ucuo-Shuanghu (L SC Z ) and the C hangning-M englian (C M C Z ). cam e assem blages. T he granites are of S-type in the N anling I’h e accretional zones com prise the Jinsha}jjang-`Fengtiaohe (JT A Z), R anoe, and ol'S-1-type in north-east C hina. I he volcanics se em the G arze-Litang in T ibet and Y unnan. A lm ost every zone is accorn- to have been form ed in an active continental m argin w ith rela- parried by a m agm atic bell, consisting of subduction- and collision- tively thick crust. as they show clear com positional polarity type volcanic and granitic rocks aged from L ate Perm ian to Late T ri- across the m agm atic arc in the low er Y angtze region. T he ar c assic. These m ay be called coupled ophiolite-ruagm atic arcs (M o et volcanism ceased at the end o f C retaceous ow ing to collapse o f al.. 1994 ). T he form ation of foreland type sedim ents in the w estern the subduction zone and w as follow ed by rift-related basaltic border parts of the O rdos and Sichuan basins in Late I’r iassic w as voicanism (D eng et al., 1992). 1 he granites in north-east C hin a also a m anifestation of the Indosim an convergence events in the E ast and N anling region show little relation w ith the SUbduction of Palaeotethys region (F igure 2). the P acific P late. 3 T he coastal belt contains volcanic rocks ranging in age from J3 to E l. T hey are K I-E j in O khotsk-C hukchi, K 2-E j in Post-Indosinian tectonic developm ent of east C h ina Sikhote-A lin-Laoyeling, K , in Southern K orea, J3-K 2 i n s outh- In the post-Indosinian, the tectonic developm ent of the C hinese con- east C hina, w ith an eruptive peak in K i（Fao et al., 1988). A few finent w as chiefly controlled by interaction oft he S iberian P late from andesite-dom m ant calc-alkaline volcanic rocks and I-type to north, the Pacific Plate from east, and the Indian P late from the I-S-type granites occurred in a very early stage. T he m ain sta g e south-w est. The Palaeozoic tectonic regim e w as replaced and super- (K 1) w as dom inated by rhyolite-dacite rocks and S-type -ran- im posed by the new regim e w hich consists of a C ircum -Pacific sys- ites. This is the w ell-know n 'rhyolite chain' of the cast A sian tem in cast C hina and a Tethys-H im alayan system in w est C hina, the continental m argin, w hich m ight have resulted from oblique boundary lying roughly along longitude 105'E (H uang, 1978, R en, subduction of the K ola-Pacific Plate against the Eurasian Su p e r- 1990). W ith the exception of T ibet and w estern Y unnan and a few continent. V olcanism seem s to have gradually shifted from places including T aiw an (Juan, 1994) and the N adanhada area of so uth to no rth a nd from w est to east w ith tim e . B im od al v o l- north-east C hina, w here an ocean-arc-continent regim e probably still cam e associations and A -type granites form ed in the L ate C re t a - existed, the m aJor parts of C hina w ere under an intracontinental tec- ceous indicate collapse of the orogenic belt and the beginning of tonic setting in post-Indosinian tim es. intraco n tinen tal ex ten sio n. T he m ain post-Indosinian tectoni c e v ents in east C hina include Since the Late C retaceou s, r if ting and extension have prevailed the form ation of the giant C ircum -Pacific tectono-m agm atic belt and in the eastern part of east C hina, w hich had led to the form ation of of the extensive rift basin system . Intracorifinental subduction and rift basins and extensive eruptions of rift-related basalts. T his seem s w elding w ere also im portant, as the m ain platform s and m ost of the to im ply that an upw elling m antle plum e w as active beneath the con- rnassifs had already been pieced together even before Inclosinian finental lithosphere in east C hina. T he principal rift basins in east tim e. Subduction is indicated by the developm ent of Indosinian to C hina are m ainly distributed in three belts:

石p isod es, V o l. 18, no s. / ＆ 2 14

I A w estern belt including the O rdos and Sichuan basins w hich ofN eotethys. the northw ard m ovem ent oft he Indian Platform and its have a com plicated history ot'developm ent. T hey w ere craton ic collision w ith the E urasian Supercontinent in the E arly C enozoic sag basins in Perm ian to m id-1 riassic, and becam e partly fore- m arked a change from a divergent to a convergent tectonic condition land basins in L ate T riassic as a consequence of collision in this region, and presum ably a corresponding change from upw ard betw een the SK P and the Y Z P at the closure of the Palaeo t ethys. to dow nw ard, deep m antle convection. T hey had undergone alternating active and quiescent stages in T he C enozoic tectonic history of w e st C hina w as essentially the Jurassic and C retaceous (L i et al., 1994), and cam e to an en d intracontinental convergence and subduction, and m ay be subdiv- at the clo se o f the M e so zoic. ided into tw o stages. The first stage is from O ligocene to M joccne 2 A central belt com prising the Song liao, north C hina (H uabei) and w as dom inated by strong horizontal com pression and intraconti- at记lianghan -D ongting basins, w ith filling ages ranging front nental subduction leading to the form ation of the H im alayas and PalacoI,ene to Q uaternary, except the Songliao basin w hich w a s G am idise m ountain ranges and of the giant S iw alik and m ainly C r etaceous. A ll these basins w ere lorm cd Under an lndos--Y arILin,,, Z angbo m olasse zones (Li et al二1986). T he M ain extensional or tratisterisional regirne and are characterised b y C entral 'Ihrust (M C T ) and the large-scale nappe zone in the rapid subsidence, thick basin-fill and relatively high heat flow . H im alayas w ere probably form ed at this tim e, T he rem arkable crust- T hey show in general a superim posed architecture w ith an derived in uscovite-bearing granite belts （aged 4(）一I（）M a, m ainly underlying rifting and an overlying therm al Subsidence typ e of 2(）一10 M a ）in the H im alayas and partly in Southern G angdise pro- structure. T he underlying thin crust (24-40 kin ) w as probably vide strong evidence of intra-continental subduction. In the second coincident w ith an Upw elling asthenosphere from depth. H un- stage from Pliocene to Q uaternary, the m ain event w as the quick dif- dreds of sm all faUlt-cornrolled basins are distributed along bot h ferential uplift of the Q inghai-X izailg(T ibet) Plateau. Intracontinen- the w e stern a nd th e central be lts, w h ich show to a certain extent tal subduction took place on both the Southern and the northern m ar- sim ilarities w ith the B asin and R angle type oi- w estern N orth (,in of the p lateau, and brought about the forination of the M ain M ar- A m e ric a ginal T hrust (M M I ) of the H im alayas and of the north T ibet--SOUth 3 A continental m ar(,in belt including the Y ellow Sea and the East K Unlun-H oh X il volcanic belt. T he latter consists m ainly of a C’hina Sea basins, and the m arginal basins ofSouth （hina Sea shoslionite series as \.\ell a,} a few high-K ,0 catc-alkalinc volcanic C retaceous basins w ith 山ick m arine shales ol、 pre-ritting, age in rocks (D en2, 199 1 ). T he northw ard com pression and upheaval of the the off、shore area. I fie m ain riffing phase occurred in the Palaeo - plateau have given rise to the surrounding giant strike-slip faults (lene, and w as follow ed by the N eogene post-rift depression such as the A ltUn and the H on-he (Figure 2). T hese processes have form ing asym m etric sedim ent drapes. 'I，h e Pearl B asin and th e produced rem arkable effects as far aw ay as north-w est C hina. Q iongdongrian B a、川are representative of this type, w hereas th e including I-ate M esozoic and C enozoic m olassc zones developed in tecton ic c haracte ristics o f the B e ib U A an B asin a nd th e Y e llow the Q aidani B asin and along the northern piedm ont zone of the K un- S ea B asin fornted o n a con tine ntal b ase m e nt show sim ilar c har - lun and Q ilian M OU111ainS. 'the developm ent of foreland thrust belts acteristics to onshore rift basins. The m ain continental m arginal in northern Tarfin and in the Junggar and T Urpan-H anu basins in basins of C hina w ere developed on basem ent ofenher com m en- north X injiang w as the result of com pressive forces acting from e ither sid e o f the T ia nsh an M o untains. ta l o r tran sitio nal cru st (L iu e d.. 19 9 2). A s m entioned above, C enozoic inaaI rn a t ic cvcnts are charac- tcrised by rift-related basaltic eruptions, w hereas granites seldom occur in east C hina. PalaeoI-cric tholeiitic basalts are found beneath C oncluding rem arks the sedim entary beds in m ost basins. and m ay im ply a relatively fast spreading, rate for the basins in the Palaeo-enc. O n the contrary, the I．C hina is a com posite com m ent consisting of nine tectonic N eogerie-Q uaternary basalts are characterised by peridotite nodule- dom ains that w ere sutured together in different stages. 'There have containing alkali basalt series. T hey occur usually as individual vol- been five m egastages of tectonic evolution, am ong w hich the end cano or volcano clusters. and probably denote continental rifting- Jinnin6 an and Indosinian stagIe s m ark the inost im portant changIes in w ith a relatively slow spreading,I rate (C hi, 1988 ). the tectonic regim e. 2. Prim ary continental crust 丘-irm ed scattered PrOtO-11LIC16 in the E oarchaean m ainly in north C hina, w hich coalesced into separate Post-Indosinian tectonic d evelopm ent of w est C hina continental nuclei at the end of M esoarchaean (2.8 G a). T he conti- the elim ination of Palaeolethys and the form ation （们 he Eurasian nental nuclei com bined together, first at the end of A rchaean and Supercontinent through the convergence of continental platform s then in the Palaeoproterozoic （1800 M a). to form extensive prolo- and m assifs, m ay im ply that, in the Indosm ian StaIge . t he vast reI-ion platform s. T he continental crust m ay have then attained its largest w as controlled by a dow nw ard cold inantle flow in the deep part. In extentand form ed a loosely United Supercontinent, w hich m ight have w est C hina, the generation and evolution ofN eotcthys w as the m ost been a part of Pangaea I (T able I）． im portant tectonic event in the post-I n dosim an period. T he Y arlLing 3. E xtensional conditions m anifested by aulacogens dom inated in Z angbo oceanic basin. the m ain branch ofN cotcthys. w as probably the M esoproterozoic. and w ere follow ed by a m ainly convergent initiated in L ate Perm ian or Early T riassic, and w as fully developed regim e in the Jinningian Stage, leading to Ib rm ation of the m ature by the Late Triassic. A good suite of' M O R B s accum ulated along platform s. T he gathering of the platform s in C hina is consistent w ith w ith m afic--ulti-aniatic rocks and overlying radiolarian chcrts, and the idea of a N eoproterozoic (c. 900 800 M at supercontinent Pan- together w ith peridotites. I’h e B anggong-N uJj ia n Ig oceanic basin, gaea IT. U p to this tim e the tectonic evolution o f’ C hina had been another branch of N eotethys, probably opened in the E arly Jurassic rna in lv th e increase and sta bilisatio n of the con tine ntal c ru st. and an ophiolite suite com parable to the oceanic Crustal sequence has 4 . F ro m the S m ian to the 'Triassic the tecton ic e vo lution o i L run a also been found. T he oencral dispersion of lithosphere and the gen- consisted m ainly of the com plicated developm ent of continental eration of new oceanic crust w ere pronounced in w est C hina from m argins by rifting, splitting and reaccretion of m arginal m assit's the Late T riassic to the early C retaceous, and m ay indicate that an G enerally know n as the accordion m odel of continental m argin upw elling hot m antle PIL1111C w as in action in the deep part. In both developm ent (H uang, 1984), this is to a certain extent consistent the Y arlung Z angbo and the B anggongI-N ujiang oceanic basins SUb- w ith Sengor's idea of crustal grow th （1993 ) on the southern m argin duction started in the I-ale Jurassic, ending in the Late Eocene and ofthe Siberian craton. O n the w hole, extension prevailed in 山e C ale- L ate C retaceous respectively, T o the north of the Y arh,lug Z angbo donian, and com pression in the Late H ercynian and Indosm ian zone, along the Southern border of the G angdise M assif (G a), a con- stages, bringing about form ation of the E urasian Supercontinent. A SpiCUOLIS m agm atic belt de).eloped, consisting of calc-alkaline vol- sim ilar course m ay have occurred in m ost parts ot the w orld result- cam e rocks and granites as w e]] as m olasse deposits. 'The elim ination 1i1n19s-, jilnl the aPpPpearance （o）tT a nggaea I

M a rch & Jim e 19 95 Z5

5 . T h e c lo se o f the Indosm ian Stage saw prol'ound changes in the *Dern,, JiuIU, Y ie, D , 7hao. IT. and Tang, 1), 1992, V olcanisin, deep internal of' C hina, and the latitudinal (present orientation) processes and basin form ation in the lower reaches ofthe Yangtze R ivet tec t(）川c re glin e China I}ni\crsity ol-G eosciences Press, W uhan, 184 pp. tecto n ic g,,ram developed in the P alaeozoic w as replaced by a "D eng W anuling. 1991，The geology, geochem istry and ages ofshoshonitic 'I飞e thyan svstc]Tl in w est C hina and a Pacific system in cast C hina- volcanic rocks in the M iddle Kunlun oro&cnic belt: Scientia G eologica I’h e post-Indosinian w as tectonically m ainly intracontm ental except S inica, 199 】，no. 3, 20 1-2 13 . in the T ibet一B u rm a D o m ain . C o ntinental c o llisio n, sub du ction and 4D ong, Shenbao (S P T ung) et aL, 1986, M etamorphism in China and its Rela- indentation of' the m assifs prevailed as the three su于rOL盖nding plates, 6on with crustal evolution: G eological M em oirs. set-. 3. no. 4. 230 pp. India, Siberia and Pacific, interacted. G ao Shan, Zhang B. and Li,2．1990, G coclicnucal evidence of Proterozoic 6. A nalyses of the niaginalism . tectonics and palaeom agnelism in continental are and continental m argin i ift m agm atism along the northern post-Inclosinian tim es seem to indicate that there w as an alternating m arLin ot the Yangtze Craton, south C hina: Precam brian Research, series ol'extensional and com pressional regim es in tim e both in w est v. 47, pl).205-22 1. C hina and in east C hina, and that in the sam e period, w est C hm a and G UO ［ing/hi, Shi, Y , 1-u, IT, M a, R , D ong, IT, and Y ang. S, 1989, The Pre- D evonian tectonic patterns and evolution of south ( hina: Journal of east C hina w ere contrary in regard to their extensional or com pres- Southeast A sian Earth Sciences, v. 3, no. I科，pp.87-93. sional conditions. This m ay m ean that a convection system in the H uang, Benhong, 199 1. B iogeography（们 ate Palaeovoic llorjs ofnorthcast- upper m antle w as operating at depth below the C hinese continent ern China, in Ishii, K 一et al，cds、PrC-JUrassic geology of' Inner M ongo w ith afternatim , up- and dow n-w elling current in space and tim e I ia, C hina. pp. 159- 174. Furtherm ore, frorn a m acrocosm ic point of view , the m ore-or-less H uang, Jiqin-, 1978. A rt outline of the tectonic characteristics of China: periodical change betw een com pressional and extensional conch- Eclogae G eologicae HeN ctia, v. 71, no. 3, pp.61 1-635 tions in C hina and the seem ing ly recurrent appearance of' Pangaea Huang, Iiqing, 1984. New research on the tectonic characteristics of China: m av reflect a higher order periodic change engendered by processes C olloqia K 05, Tectonics of A sia, 27th International Geological C ongress, in the interior ot'the earth w hich w ere Under cosm ological control. M O SCO W 7. In this paper. w e have in general follow ed plate tectonics theory. H uang} Jiqitw } and Chcn, B, 1987, The evolution of Tethys in C hina and adjacent tegions: G eological lluhli}hing HOUse, Beijing, 101) pp. H ow ever, there are problem s I}or plate tectonics theorv as it no" '11ang, ChUnt'a, Yan,-,,J, Fcji&, B 一Zhu,2，et al., 1992, Opening and closing tec- stands. In particular: tonics‘）！KunlLlu M ountains: G eological M em oirs }cr. 5, no. 12, 224 pp. there is a com par at i ve lack of evidence tor ancient larIge oceans Juan, V （、，1994, Tectonic history of aiw an: Journal ofific G eological Soci and deep ocean deposits prior to the M csozoic} cty of C hina, v. 37, no. 1, pp. 1- 6- there are discrepancies in global reconstruction s o t 'palaeoconti- *IJ, Cai, 1987, The 1-,)iigiiiuctio-ShLiatigfiLi-[,itn,,can iialig plate suture and nents (the large gaps in eastern J ethys and betw een Siberia and northern boundary of distribution of G ondw ana facies of Perm o-C ai north C hina in the Late Palaeozoic are w ell know n) and honilcrous systctu in no门hein X i/ang，Ch丁ra:、J ournal ol'Changchun C ol - there are difficulties in the bio-eog aphical interpretatio n o f' ICL,C （）｛G colo.gy, %. 17 , no }, pp. 155-166 C athaysian flora in south一w estern N orth A m erica. LJ, (’h UoVU, Nkang, Q , I Ju, X 一and Tang,,Y , 1982, Tectonic m ap （）】A sia （1： 8o oo (too) and its explanantory notcs: Cartographic Publishing House Tornographic studies Of' the Upper inantle (W oo d h o use Ct Z11， Beijing. 1984) have revealed the dow nw ard extension ot'scisinic w a\ct,o r m s Li, Sitian一Yang, S} and JCF/) k ieW IC, T, 1994, Upper TriaSSIC-R urassic fore to over 300 km - w hich W ould put sonic consiraints on plate m otions. land hasin SC(ILM ICS ofthc Ordos Basin in C hina. in StratigFaphic F}olu T herel'ore it is probably necessary to investigate the extent of I'rec tion of Foicland Basins: M --lIM Spccial PUIblication no. 52. m otion （们 he cratonic lithospheric plates and to determ ine w hethei Li, Tingdon" X iao, X , Li, G , G ao, Y , air(] Zhou, W . 1986, The crustal CVO- the earth',, radius has increased in the geo logical past (O w en, 1992). lution juld uplift 11jechanisin of the Q inghai-X i/.ang, Platcau: Tect()11()- It' the earth's radius has i ncreascd up to around 15悦‘PI-eSUm ahly 川 physics, \, 127, pp.279--289 an episodic pulsatory and asym m etric w ay (M ilanovsky, 1983 ). the I}i. X in&xuc, and Shen, G } 1992, Perm ian phytoprovincialism in the Far Fast: discrepancies m entioned above m ay be reconcilcd.川 cast ［（）a cer- Palacontological Society of Korca Special Publication no. 1. pp. 1-26. } IALI, Baojun and XU, X , eds，Evolution of the sedim entary basins and their litho- t, 川 I e x te n t. 1是Icle、1）之11是Ic（）gc（）gr之又1〕11y O f } outh C hina: Science Press, Beijing, 236 pp Liu, Benpci. I'Lng. Q , and Faru } N, 1991, Tectonic evolution of the Palacolethys 川Chang川ng -M englian belt and adjacent regions, western A cknow ledgem ents Y tiiiiiiii:Joui-n}ilol'('Iiiiia U iiiversity ot(;cosciences.},.2,pp.18-28. Liu, D , Y, N utinan. A , 'I几〔orripston.W ，W U. J, S, and Shen. Q , H ,1992, Rcinnant of＞3800 M a crust in the (’h inese pait ot'thc }ino-Koican Cra W e are thankful to C lient, Y uqi. D en- lint'u, D ong S henbao, H e Ion: G cology. v. 20, pp.339--342 G Uoy , Li Sitian. Li T ingdong, L iu B cipci, L iu H efu, R en JishUn, Liu, G uangcling. cc｝一1992, M ap scries of ucolog} and geoph". ics of Cluna Sun S hu, 'Y ang Z Unvi and Z hant, Benren for fruitful discussions and and adjacern regions: G eological Publishing H ouse, Beijing. to Shi X iaoxin(}, Li X ianL, and Z hao Y udong for help in VarIOUS M a, X 111gyLlan and W u, 1), 1987, (’c nozoic extensional tectonics in China: w ays. T he references had to be very concise, and it is im possible to Tectonophysics. no. 133, pp.2-43--55 list all the papers and Publications consulted. M ilanovsky, F.E，1983, M ajor stages of riltimg. evolution in the earth's his tory：一「ectonophysics, v. 94, pp.599-607. M o, X uanxuc, f)en,(, J. and Lu 「，1994, V olcanism and the evolution ol' R e fe r e n c e s Tethys in Sanjiang area, southwestern China: Journal Of Southeast A sian Earth Science,,, v. 9, no. 4, pp.325-334. * in Chinesc Aith FnLlish Sum m ary, others in English O w en. 11 G , 1992, H as the earth increased in size'! in Chatterjec, S. and Hot- ton III, N , cds., New concepts in global tectonics: I exas Technical U ni- Chang, C hengla, and Bian, Q . 1992, The 1111.11ti-branched orogenic com plex versify Press, Lubbock, pp.289-296. of' the Inciosinidcs: nature and evolution （）「Palacotethys: Advances in *R en, Jishun, （hen, T , N iu, B , L iu, Z . and L iu, F , 1990, T ecton ic evolution G coscience (2). C ontributions to the 29th IGC , 1992, K yoto, Japan. and m ineralization OF the contincrital lithosphere in eastern China and C hina O cean Press, pp. 1- 9 adjacent regions: Science Press, Beijing, 205 pp. Chen, X u and Rong, J, 1992, O rdovician plate tectonics of C hina and its Sengor, A M C , N atalin, B A , and Burtinan, V S, 1993, Evolution of the neighboring, regions, in W ebby, B D and Laurie, J R eds., G lobal Per- A ltaid tectonic collage and Palaeozoic crustal growth in Eurasia: N ature, spectives on O rdovician G eology, pp.277-291 v. 364, pp.299-307. *Cheng Yuqi. chief ed ，1994, The rcgional peo〕logy ‘）｛C hina: G eological Sun, Dazhong and LU, S, 1990, Tectonic evolution ot'the Proterozoic in the Publishing H ouse, Beijing. 507 pp North China Platlorni: in N aclvi, S M , cd., Precarnhrian continental crust C heng, Y Liqi, Sun, 1), and W LI, J, 1984, Lvolutionary m egacycles of、 the Early and its eCOuO111iC resources: Dcvciopm ent of'Precainbrian G eology, v. 8, Precam brian Prolo-NoFth C hina Platform : .101urnal ol'G eodynam ics, v. I， pp.503-522 . T ang, Kedong arid Y an, Z, 1993, Regional m etam orphism and tectonic evo- p p.25 1-277 *C hi. JishanL ed., 1988, The Study ot"Ceno/.oic basalts and the Upper m antle ot lution of the Inner M ongolian suture zone: Joum al of-M etannorphic G eol- eastern C hina: C hina U niver}ity ol'G eoscicnecs Press, W uhan, 277 pp. ogy, v. 11, pp.5 I卜522.

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*Tao, K uiyuan, 1988, The B asic characteristics oft he M esozoic volcanism i n Zhang, Benren, Luo, T, G ao, S, O uyang, J, H an, Y , and G ao, C, 1994, Geo- the coastal region of southeast C hina: Bulletin of the N anjing Institute of chem ical constraints on the evolution of N orth China and Yangtze G eology and M ineral Resources, no. 9, pp. 12-30 blocks: Journal of Southeast A sian Earth Sciences, v. 9, no.4, *W arg, Hongzhen, 1981, G eotectonic units of China from the view point of pp.405一16. m obilism : Earth Science- Journal ofW uhan College ofG eology, 1981, no. 1, pp.42-66. *W ang, Hongzhen, 1982, The m ain stages of crustal developm ent of C hina: Earth Science- Journal of W uhan C ollege of G eology, 1982, no. 3, D r H ongzhen W ang is a p rofessor 15 5 - 17 7 . of the C hina U niversity of G eo- W ang, Hongzben, and Q iao, X , 1984, Proterozoic stratigraphy and tectonic sciences (B eijing) and a m em ber of fram ew ork of C hina: Geological M agazine, v. 121, no. 6, pp.599-614. the Chinese A cadem y of S cience. H e W ang, H ongzhen, 1986, G eotectonic developm ent of China, in Y ang, Z unyi, w as form erly the P resident of the C heng, Y , andW ang, H , The geology ofC hina: C larendon Press, O xford, P alaeontological Society of China, pp.235一75. and has specialised in coral palae- *W ang, B ongzhen, Liu, B , and Li, S, 1990, G eotectonic units and tectonic developm ent of China and adjacent regions, in W ang H ongzben et a]., ontology, p alaeogeography and Tectonopalaeogeography and palaeobiogeography of China and adjacent P recam brian geology. P resently, he regions: C hina U niversity of G eosciences Press, W uhan, pp.3-34. is engaged in the stu办 of s equence W ang, Q uan, and Liu, X , 1991, Pre-Jurassic tectonic evolution betw een stratigrap 勺 of C hina and on the C athaysia and A ngaraland in Inner M ongolia of China, in Ishii, K et al., reconstruction of palaeocontinents. eds., Pre-Jurassic G eology ofI nner M ongolia, China, pp.99-112. H e is also interested in the history of W ang, Tingyin, W ang, S, and W ang, J, 1994, The form ation and evolution of geology and is a Vice-P resident of Palaeozoic continental crust in A lxa Region: Lanzhou U niversity Press, IN H IG E O , IU G S . Lanzhou, C hina, 213pp. W oodhouse, J H , and D zievonski, A M , 1984, M apping the upper m antle: Three dim ensional m odeling of earth structure by inversion of seism ic P rofessor X uanxue M o is D ean of w aveform s: Journal of G eophysical Research, v. 89, pp.5953-5986. the G raduate School, C hina U niver- *X iao, X uchang, Tang, Y, Feng, Y, Zhu, B , Lin, J, and Zhao, M , 1992, Tec- sity of G eosciences. H e has under- tonic evolution of northern X injiang and its adjacent regions: Geological Publishing H ouse, B eijing, 169 pp taken studies on igneous petrology, Y in, A n and N ie, S, 1993, An indentation m odel for the N orth and South volcanology and tectonics, esp e- China collision and the developm ent of the T anlu and H onam fault sys- cially on Tethyan tectonom agm atic terns, eastern A sia: Tectonics, v. 12, no. 4, pp.801-813. analysis, in Tibet and adjacent Yin, H ongfu, ed., 1994, The palaeobiogeography of C hina: O xford U niver- regions, and on C enozoic peridotite- sity Press, 370 pp. bearing basalts in eastern China. *Zhang, G uow ei, et al., 1988, Form ation and evolution of the Q inling O ro- genic Belt: N orthw est U niversity Press, X i'an, 192 pp. Zhang, H uinnin and Zhang, W , 1985, Palaeornagnetic data, Late Precam brian m agnetostratigraphy and tectonic evolution of eastern C hina: Precam - brian Research, v. 29, pp.65-75.

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