Ited Eeds" of Yunnan

By

M. N. BEEN(Ce,ioz'oie I?searc1z Laboraioiy, Gcological Survey oJ C/u/id)

\Viih S Text-Figures tad 3 Plxtes.

CONTENTSiNTRODUCTION..................................................................GENERAL CONSIDERATIONS ....................................................PREVIOUSWORK ................................................................PRESENT UNDERSTANDING O!' THE "RED BEDS................................RECENT OBSERVATIONS ........................................................THE1.UFENG AREA .........................................................

A. Stratigraphy ................................................................paleozoic ................................................................

Sinian ................................................................Mesozoic ..............................................................

Upper TrizssiC Ipinglang Cl Series ....................................Upper Trissic Lufeng Series ..........................................?Jura-Cretaceous Shihmn Series ........................................

Cenoroic .................................................................Plia-Pleistocene gravels and sends........................................Quaternary deposits ....................................................

H. Structure ....................................................................TILEANNING BASIN .............................................................

A. Stratigraphy ................................................................I. Paleozoic ................................................................

Sinian ................................................................Lower Cambrian ........................................................Lower Carboniferous ....................................................

Ihcceiveti tar pubIktion in .\pril 1941.

Anthracolithie .......................................................... 'so

Upper Perinian ........................................................2. Mesozoic ................................................................

8181

Upper Triassic Lufeng Series ..........................................?Jura-CretaCeOus Shihmen Series . ..................................

SI82

3. Cenozoic ................................................................ 84Plio-Pleistocene deposits ................................................ 94Quaternary deposits .................................................... 94

II. Structu re ...................................................... 14

THE SHSHAN SYNCLINE...................................................... 88TUE SUNG}IUAPA BASIN ........................................................ 88TIlE YANGLIN SYNCLINE ...................................................... 83THE SHUITANG OVERTURNED SYNCLINE .................................... 89

0111ER PARTS OF THE LAKE REGION ......................................... f19

THE FUMEN OVERTURNED SYNCLINE ........................................ 90FROM FUMIN TO VUANMO BY WAY OF WUTING 90FRÙMYUANMO TO LUFENG BY WAY OF YENHSING ........................ 91

01'IIER OBSERVATIONS ........................................................ 91

LED BEDS" OF EASTERN YUNNAN ..........................................RESUME OF RECENT OBSERVATIONS .......................................... 92

DISCUSSIONS...................................................................... 94The stratigraphic position of the Ipinglang Coal Serie ................................ 94Th,i diverse nature of the "Red Bads'' type of deposits .............................. 'HPnct-Shihmen oragenic novenunt, Yettahanian or Hengyangian? ........................ 95

9f1hEFERENCES ....................................................................

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,Vetvru Vunnut va' iir:.t made ní,\'l rsou'k rhe rïeeot vort' -

Btu»,:fl . Assone the n'h e1logistS, fh -re re [)e1,r J W, ardJ. Grcgiirv. T. û. Chu, A. Ceso. N. Krelci -Craf, W, Crednr and E.

'aurin, who have all expresed thnir o p!nïons. u cernins the ago and thearruetu re o such beds.

The term "Red Beds' has been purposely p1-aced between quotation

rnarbs svrh the e.pithet 'so-called." in front of it, hecause this tern bac neverbeen applied in a resricred sense in China. Formations sindut this general

term, though of differeri. ages and in tuitterd geographic positions have actuallybeen broadly correlated. su-eh as the attesnot made by Kisata Chan t ]'

This osper is not an exhaustive treatise on all th ''l{ed Reds'

Yonnasi and has no aseeruon r) such claim. rhouTh ose mi'ht perhaps be ledto mhicve ho its generalized title. It is the purpose oi this studc to lay our

the problems concerning the age a id the structure of the so catled ''Red Bedsof Yunnart which are brought out by the dscovery of deteminahle Saurischian

and trimitive Mammalian remains from these beds as Luftng2 irs the central

part of this province by Technician T. Y. Wang arid myself in I93R [3.Thereby. from now an, we cannot rcgad the ''Red Beds'' as unfoceiliferous,

As a matter of fact, this hai eventually opened up new vistas to thc solution oftIe age problem of the 'Red Beds' of Yunnan which has been hitherto tls

suhJeei of conrroversial views for q tute a nuniher of years

The discovery uf determinable fossils, at the same time; has acted as anlucentive for further suidies of these interesting 'Red Beds'' which are saliferon s

at different localities. Consequently, C. C. Young an'.) myself have again visitedthe Lufeng Area after a shirt reconnaissance in the Anning Basin towards

aud cii 1939. This trip resulted in a better understanding on the geolôy orthat region and the collyction of additional fossil material.

At tite beg j niai ng of 1940, detailed geologic Survey of the Kunmiug

Focicuns lias ulreadr» comuienced, I have ioincd the held arty arsd collaborated

: s n rs ss pa rS 'Te r r I5etr.i'Ct'- id i,l psp.i

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Fig. 1.Iudex sup of Vuimar,. showing the niajor drainage systeim and their divide

and the kcatiois of descri!'eI areas.

I am greatly indebted to Dr. C. C. Young for his 5turly and determinationof most of the collected vertebrate fossils under a condition which is by no

mean, facorable and pleasant for such work. Furthermore, he has given mehis untiriug arlvices arid constant encouragement during the preparation of this

encre. Tn yy enfleanes. notably Mcsrs. T. Y. Usu, C. S. Pien and ¡IiqChinqcltang I am cytr,nie! graefu1 [or their hearty collabotation in the field,

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Red Reif; ' nf s't1!t17O' 159

wit! L Y. Hsu C. S. Pico and i3iq Chi nchatig in the ma1dos ot the

Annh', [tasili and several other muir areas where ''Red Bcds" are involved inehr- si ructrtres around Kunining. This work is stdl in progress and otore data

on the "Red Beds'' will eventually he accumulated.

¡hillc:in of !ie Gcu!oc;l oe,eiv of CJim: [ Vo NIX î,

the shariu4 01 LuCir ideas, and the buieit (i iher trank dtscussons lianksaie aLio duc to Nir. Y. S. Chi who has helpcd me through many ditlicuhits Lvlooking up references which are not available here in Kunming and also by hisunbiased dscussons ou certain problems concerned in this paper through

:o r respondeflce,

UL3NERAL CONS1DERAT( OMS

Yunnan, the southwesternmost highland province of China, exhibits sonicstriking geographic and geologic features of the earth's surface. lt is a regiondrained Lv seven major ricer systems (see Fig. ). The rivers on the west ofthe Lu Range' , the Saiween-Mekong dia'ide, find their ways to the Indian

Oeean, while those on the east empty their waters into the Pacific Ocean.

The great rivers of Western Yunnan, disregarding the tributaries of theIrrawacldy, such as the Nmaikha, the Malikha and the Shweli Rivera, show amarked parallelism in Northwestern Vunnan and its adjoining region in Sikangextending across a stretch of land more than 2 degrees of latitude. lt is the

region sometimes styled as the Faiccau da Mekong where the arterial elementsof the Yangtze 4Chinshachiang)3, the Mekong Lantsangchiang)', the Salween

(Luchiang)5 flow within a short distance of each other with the mighty

Tahsueh and Lu Ranges laetwcen them. To the south, the former river turns

abruptly northward at the Shihku' bend north of Chientsuan', while the lattertwo continue to Row southward but gradually diverge from each other.

The Yangtze in Northern and Northeastern Yunnaa first flows eastwardthen turns towards the northeast into Szechuau making a southward bending

loop with the apex extending a little south of the a6th parallel around the roardmeridian north of Yuanmno'. The drainage pattern of the Upper Yangtze withits hairpin bends has led many geographers to speculate on the theory of

diversion or river capture for the origin of this great river.

In Eastern Yunnati) the \Vcst River (Nanpanchiang) also assumes the

shape of a southward bending ioop, but it is more compressed than the one of

the Yangtze True karstic topography with underground streams of the lime.

stone terrain abounds in the drainage area of this river.

I lt; 2. a1t;3. uit; 1 im:; 6. J; 1t ¿ti,

7. ?f; 8. JI; 9. 5; 10. iiJ

Between the i eridind rivcr courses u the Saiween asi(i the Mekong onthe west, and the loops of the \'angtze an3 t he \Vci River on the norththe northeast, the intervening area in the form of a dvctail is occupied by thesoutheasterly courses of the Red (Yuanchiang) and the Black (Papienl1iang)tRivers with the imposing Ailao Range3 bctweet them. One striking feature j

this area is the occurrence of one of the greatest fractures art earth. It j

conveniently named the Red River Fault by f-I. M. Meng [ao, p. 430], becausei tOilosvs, more or less, the course oí that river. This fault has forced up a

belt of Archean rock on the southwestern side of the Red River composing thenorthern stretch of the Ailao Range and also the Tientsangshan' at Tl'Some of the earthquakes that occurred within historic times and up to thepresent days in X'unnan which show crustal instability may be caused by rccurrsntdisplace nents along this great fault. It extends southeastward into Indo-Chi rutand northwestward to Tau. Probably it runs continuously along the UpperYangtze above the Shihku bsnd as fir nort'i as Pain (Batang) in Sikang oreven further.

The lake region of Yunnau lies between Kunming and Kchiu1. Thelargest lake Tienchih (Kunyanghai)' is drained by the Tanglangtsuan', upperreach of the Putuho' ° which is an affluent of the Upper Yangtze. Other:tkes, such as Yangtsunghai' ' , Fuhsienhu' Hsinyunhu' ' , Ctiiluhu'Yiiuoghu' etc. all belong to the West River drainage and most of theni areprobably of tectonic origin, though karstic processes might have played a pLut

in their formative history.

In Western Yutinan, the well-known Erhhii' (rali lake) which lies

immediately to the east of Tientsangshan belongs to tite Mekong drainage.This lake is said to be mainly of tectonic origin.

The distribution of the ''Red Beds'' in the tliffercrit drainage areas is

very extensive, Coggin Brown says,

f2ast of the Mekong. a great part o! Centrai Yunnau is coered by t formation its -ht-ht!ossliifero'c; red sanistonas and simles predominate extendin7 over thousands ttf 'tque'e tiiletd occuoyin a much larger sut face area than other group of rocks.........

1. 5i7/j:: 2. 4j; 3. 4j 4.jtlIj: . *ll 6. t'.'7- f; f. 9. Ji: H. if.j,f; H.

; 12. f111 'i: 13. . lt. [i i 1. ff . Is. fif

'1os. 211 Rsf RJc 'l/ii11(' 1 íi

Otuj a;tirt,

'West of the k:trstic refion uf Eetr.ro 't5FOtI, it e,erV ]lretiufl ttave5ted huth t, titeaud to ties south of the Tall Fu.Vurtna,t Fu route, t titi tite lied Beds (4, p.

and p. 5L5).

Hr has also divided the areal extent uf the ''Red Beds'' into (i The

Subsidiary Red Basin in Yunlung iii the west and (ii) 'The Central Basinand Other Occurrences' on the east, but not as two distinctly separate basins,because he has warned us a gsiuct acquiring suck an impression hy saying.

'It is doebttttl if the Yttolung Basin is a orate est be as tome geologists have supposed¡e tust ptobahly s subsid arg p'ctloisttite tesvaed; the west of tP,e na iii basin uf Gen; e;Y,nn;us, (t,

The dic'oskion of the outcrops of ''Rest Beds'' ¡s inteestinq. Aroundthe lake recon, they are either roughly crescent-shaped or in narrosv andelongated strips. The latter ones generally strike northnnrtheast-souzhsoutb werttu northeast southwest. They occur as separate patches surrounded by olderrocks, To the west, the outcrops in the Yangtze, the Red River, the Black

Rver and tht Mekong Jrainage areas arc practically continuous over bOb.tretches when going across the general strike of the beds, though occasionalold rock harriers occur between them. They are either gentiy inclined orvigorously thrown into a series s.f isoclinal folds. In the latter case, one usuallygains a false impression of the apparent thickness of the ''Red Beds''

PRVOUS WORK

A hstorical srnnniary of the opinions of previous observers on the ge

of the ''Red Beds'' of Yunnan curl a comprehensive bibliography of papers withdirect or indirect bearing on that problem has been iven by J. Coggin Brownin t 938 [ ). The liberty of orn itting some of the papers referred by him fromthe list f references at the end of this present paper has been taken byassu sting familiarity with the afore-citel work.

A brief and condensed summary OF previous opinions will be given itere,

bum' of the works not mentioned by Coggbs Brown cre added, Generally

spe:tk;ng. there are three groups

.12

i ) lc 1ir; g ru ch 1 tImer who r»eari mLr:,j :mkn: mr Pr d.im md Tihissir: mr rrm>hn r 1'rimt.sic; or Pero'..

scmr o: :ge. L. von 1r,c7v, h. A. Duelas, 'el. A. Ï.ecLre. f. D:nr.n.. .\

T.reeimdre, J. (Thgttn ltrûvo. f. W. and '. 1. 'regnry, aol T. C>. h»

rj bj>0 to tbk rommg.

Chu proPnetl the lam: mmning Foreti on For dme ''Rel Ped'. I o

al the geolomzic mips and .s'cdnns arcompan ving his work, this formatiom'

sipnated as of undifTerentiated erndai a'e, but in the tet:t hr has ah ibto im s being prohabb? \1ccozrdc.

Coggh: Brsmvn ci es 1 tI>> euId dLV>St')fl tI,. 'RÇ'CI i'((rcrtsidemhig these to he lying st..' atigrmm hic;iuly- htwcva t he (ggrm!op'r,l.oímigian) below and thr col ma.sure. o Yorm ini1 (Node) aTor.- he aid yes

at the conclusion that

'the Rai Tte' > .iuestkn ca'>> t i -hier than itpps Perot tad est s t,1or ttiam> t

t'ee' Titas..."I, p. 1fl

Lie believes the Lopingian to he Middle Permiarm. Thc coal measures of Yunnimk

which follows the narine Carnic and lower orie beds of Miaorsway (Miantsut>

'e>rhu1 any distinct break hear the following dorai elements which are

determined by A. C. Seward and published by P. Sahni [ :3. p.

.oc I. Tunean Fielen (H. i,mi>gvnn) 4

.'Psilozamjis di/ans Precl Braun

Pedoramit,s lanrsoI'Imm; I . & H.)lace rttte

ci:. 2 .'Miaotsway il icciteni.)

Euice.rites .Snani (Zejfl. ,

T>ieivûpl:v/ltii..R sss.. ti..,

Timeni'íplet'is ¡Oiiis/t'J t. /,ejil. '.

T)ic/vs,f'/ ml/tija .Vmi/i «s/i (Zeill.),

(,'eadOts ,Cahalss.i (Zeii1 .

T'rle.i>de,i Zilll sp. n iv. (This jeu-m d>mbt ideritica hitlm Zejltre euH >.Vo' 55rai1mlîis His/n pl trou> Tonkin).'

.>rdisg this i>rm, C.gici Biown remarks.

];i/iío o! t!i, fiJoiüI enciele of {; [\nl x;'<,

par tie out; l'oi u;k f lora h ,ie U y r'au;luii as Rhact je, is now placed in the Noria s

icteeil, the \iii'it5SV5Y ettOi' fti5RKIt IIUOIL&1 piouf that this change it correct.''p. 541)

I le also correlates the cool measures ol Yuunatti with the plant beds of

Cisennan' and Tpinglang2.

The junction between the marine Trias and the ''Red Beds'' proper atYuniiani was first stated to be a fault contact, but later considered to be dueto lateral variation. Coggin Brown definitely regards the coal measures of

Yunoani to be capping the 'Red Beds'' is quite manifest in the followinggeneralization on 'the events associated svith the formation of the Red Beds''which states that

later events in Central Yunnan belong to lacustuine and continental registe; culminai ¡oin th Norisn.Rhaeuic coal measures.'' (-h, p. 567t)

(2) 'flic second group is represented by E Saurin [24) alone, whoconsiders the ''Red Beds" to be mainly Upper Triassic in age.

Saurin's observations are confined to the region between Kunming andYuanyungching (I-Iouching)3 of the Knangtung district which, more or less,corresponda to the Lufeng Area and the Anising Basin described in thepresent paper.

According to Saurio, the ''Red Bcd'' arc composed of a ''poutlinquede base" followed by ''couches versicolores, argiles lie-de-vin,'' and ''grrouges supírieurs horizontaux.'' The latter beds are said to be the lateral faciesof the coal-bearing strata of Ipitiglang which bear the following plant remain;:Podoeamikc distans Presi., Clathrople.ris pintyph y/la Cuepp., and Taenia pte»iicf leclerci Zeilier. These beds arc supposed to be moulded on an aniclinaI archof the 'Red Beds" and considered ro be Rhaetic in age. Although the basalbed rests on a vari-ihie substratum, yet tite ''Red Beds'' cars he definitely said to'be post-Permian, because they overlie tite limestone that bears Neoschwagerina/nzíc';/leu Ozsva near Kunming.

Fossils from the ''Red Beds'' proper are found near Aiming. They areFstI,eria sp. and Esher!a cell/i Marssuy that are considered to be ot little helpIn dating tise beds, but of interest in corre1atig the ''Red Beds'' of Yunrian

with those of LTpper Laos in Indo-C'i;ii which bear the sante fossils.

I. ¡j-: 2 - 2F il 3. i: -Je .

1, *L 2. **; 3.

Allowing a prolonged period of cr031/li nid. at I3.c, j)«/(5iiltt' e

atcr the Anthraeolithtc ti/sse and hfre the deposition ot 'Red Bcda.' i ii

might have taken the whole span from Lower to Middle Trtassic, S;ierin rYnt.sr1-c:

(Jo peut donc conclure è I 'áe rs iasiq lie moyen et su péricur, ou Oculen Slit S' .ul "1du terrain rouge plissé (couches versicolorts, argiles liede-vin, terrains saiiIrres moansda,,s le Garniert) et l'âge norien-rhétien des iès rouges snprieurs hoiiontauic.' (24, p.

On the structural relations of the ''Red Beds,'' Saurin makes the follcwirscobservation:

''Les grès supérieurs, de iii que les concises rhétie ones a charbon et . plaittes, soothoriramtaux. Le fait que ces dernières, datées par leur flore, n'ont pas subi les plissements3tintaiayens, itsvqués l'ai Credner, Heim et Krejci-Grat, est un argument pour attribuer aucmouvements néetriasiques Je pJissment des couches sous-jacentes, er celles-ch par suite, auTrias." (24, p. 48)

() The third group that considers the "Red Beds'' to be Crctaceous5

Oi Cretaceous and Tertiary in age, and, at the same time, advocates tIse

importance of the Himalayan movement in the tectonic history of Yunnan, is

composed of A. Heim, K. Krejci-Graf and W. Credncr.

Heim and Krejci-Graf [isj made their observations along tite route

from Kunming to Szechuan by way of Fumin' and Huciii3. The ''Red Beds''studicd arc regarded to be analogous to those of the Szechuan Red Basin andhencc of Cretaceous age. Most of the geologists who worked mainly in Szechunand Sikang are much inclined to this opinion.

According to Coggin, Brown, Heim has later withdrawn his previous

opinion and considers the "Rd Beds" around Kumning to be probably Pernio-Triassic or Triassic, "because they directly overlie igneous horizons correlated

with the Omeishan basalt.'' [4, p. 524)

Krejci-Gra in a later paper of his own r'} has divided the "RedBeds" of both of Yunnan and Szechuan into a lower and an upper group withno distinct angular discordance between them. The lower group is supposed

to be of Cretaceous age and the upper one as of Cretaceous to Tertiary. Of

structural interest, he has shown two overthrusts of Anthracolithic rocks overthe "Red Beds" both at the Yangtze and at Mati3 in the geologic sections

N's 2 41 Ii7r.--''Jsa Is(L, VI np,i,, 113f;

''I

lÇo'l.'' fl l. \iI. a]. 1nr lina t (, gout with W1IILII I j \ eohflorator

Ps. tidii r's [ç trac crc ir extenithe Vrst2rl) ( Vuidw rsr. lbs tI II

A ijl he crue: ore ot tise ''ked h t .it1d U Oui hi 1 lotit t

thc rout l'ctv'rru Fttnm ASpi ïi 5CiA.CU5S1IÇ Lu feu. Pi cced iroua Yaorhaiu lo Lufemt ou Usc row tjvered. Ot prrel bu tb Yunnan

Burnu:i loligliwav l see Pl. L figs. r, , and ), and then striking westward j 010

the hills, he lias made certain geotnurphoiogic observati0115 Apparently basiuo:ioon ihcse observations, lie hat constructed the schematic sectjon ficar Lufeu2shown by fig. e or fig. a of pl. viii of his paper. ibis critical sectionshouv a liagraut unconformity between two red formations and appended withan interpretative explanation as follows:

Fnconfrruiiity bot ose iBs oidor folded K_ui bOuL íd the Ycuger Jed Bed SInISa: ion,decrease of the intensity of di towards tie E in the latter hQw5 that tile deausit ion otyounger Red Beds has gotue on du ing the Ceasing ut itIC last folding movemenns.

The "elder raided Resi Beds" are considered to be of ''Mrsoaoïc. probablyiouager Mesozoic age while ''the at laying Red Bed formation of Lu Fuue''is regarded as of "Middle and Upper Tertiary,'' because the sharp unconformitrbetween the two is looked upon as the evidence of ''the intensive Himalayanfolding.''

Later works on the 5Rcd Beds' may now be mentioned. M, Y. Fucoin i93 has found determinable Upper Eoccne vertebrate fossils from the ''RedBeds'' oí the Lunan Basin 2) previously regarded as of Permian.

H. C. Wang 28) in his study on the geology in the environment ofKunming fl 1939 has divided the "Red Beds" invoved in the Shshan2syichine into a lower and an upper group supposed to be separated from eachother by a conglomerate. The lower group is regarded as of upprnsoetPermtan age cafled the "Anfing Formation''. after the name proposed by Chu,On the strength ol one single plant foss!, Equsetacs sp., the upper group s

correlated with the Ipingiang Coal Series and considered as of Jurassic ( ?Liassic yage and named sise '' Ssaopuchi3 Foi ination."

I, X 2. tt iii; 2. J. .

4

()iher g i.ic .slco ccv i, ç i.cnj c: t;

L.tl&idfl differ in tiier opinion: coced c he age th 'Red UJs Lc

utking, the :cgd assigne1 t j', .lflg cci PecjariPRESENT UNJThRSr1ND:NG OF TW "REt) BiUS'

u accvcc nl tile i15eOer u. 'I'riassc eaucis i and pritiet rcnsacn; at Lufcng, the gLgie secr;on there ii been c egarded i

a iandard for cocuparisoo and ctrehcuon sjih 10cr 1ocsJ hics where

Lieds' arc involved.

Elsewhere (, Pi. I] I ha :e gvcrt iic Lu Scctiícic. The "Red Beds'are divided into a lower grouo. the Lucng Series, which is disconformabivuvcrlain by an upper group, the Shihmen' Series. 'I'he Lcifeng Series is

turn subdivided jut, a Lower Carnosauria- and Bccouiicrc:r;-hcaring Senies aujan Upper Hybodus- and Ltnionid-bearing Series.

Tite Lower Lufeng Series is dated by its fossil contents to be UggeTrkcssic in age, while the Upper Luieng Series with its less characteri'tcc ;'ussi

cvideñces can stilt be regarded to belong to the sa;a scqucncc: and age.

The upper stratigraphie limit of rhn 'Red Beds", represented by theSicihinen Series, is not well-detinsed, because ria fossils have, so far, been foundin this series. It is flow tentatively considered as of jura-Cretaccous age.

For the present, it suffices to say that by using the Lu Htg Section as atype section for detailed comparison and correlation of the hthulogic as sycil a

the stratigraphie characters, it has been found to be satisfactorily applicable to

areas investigtcd up to the present.

RECENT OBSERVATIONS

1eccnt observations on the ''Red Beds" of Yonnais have hecti pmO ictedto celtain arcas, such as the Lufeng Area and the Auning BaBti, a ivc-li as

ticosc acquired along routes tiarersed during various ountccys in this provo'.. e.

Tb ir they will be described as separate areal and route ob,cr'ation.s,

TUE LUFENU AREA

The location of the Lufeng Area is shown in Fig. t .. cntisprehensL'e

cccture uf the maui topographie and structural features could he gained fron

1j Ii.

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Nos. 2-4J ßcu:....kcd Bcda o! unou,i 169

au inspectIOn Qt iltc Eicld ketci 1l. 1), tiR. block d .gra us ) mire

geologic map (Pi. 11) nl: this aiea.

A. Stratiraphy

PALSOZOI;

ite uicro3 ) SWOLIl ohiUl i(CuJ IJ(ai) ttIi WJ1il

act as a narrov barrier between the two cNtCiiSVC regions J 'J which

are differently dssposcd structurally. They comprise of josrplc phyilitcs, o hita

quartzites, crystalline liniestones, and roica and caic-schists. Xt plac C,

rocks are penetrated by numerous quartz veins which are crushed ami1 COOtOtted.These beds arc sometimes highly contorted both horizontally and vcrticaliy.

This lias rendered the detrniinatioa of iormal succession o these beds rather

dillicult. As they arc either in sharp unconformable or fault contact with theoverlying Ipingiang Coal Series or Lufeng Serics of Upper Triassic age, their

exact thickness cannot be determined.

The Sinian rocks of this area are distinctly the northern extension of

thoic with iron ore deposits of the Irnen district which has been carefully

studied by Y. S. 1-luang in 1938 [I6. They may be corrclatcd with Coggmn

Brown's Kaoliang Series as suggested by Huang.

2. Msozoic

UPPER TRIAS5IC IPINGLLNG COAL SEinES. The geology of the coalfields

of the Epinglang region. has been investigated in detail by H. S. Wang, T. CChow, C. H. Lu, Y. S. Huang and C. C. l'ai of the Geological Survcy ofChina in 1939, but unfortunately their results have not yet been published. The

generalized succession of beds in an ascending order may be riven as follows:-

Shales interbedded with ooarse arkosic sandstones; coarse arkosic sandstones with yellowish-brownshaly layers that yield numerous plant remains; black shales with occasional layers thatbear abuilant small pelecypods; massive coarse arkosic sandstones with occasional

conglomeratic layers; grey and black shales vcith numerous plant ressiains occasionally

embedded with lenses of arkosic sandstone; loose black and grey shitles with sandstone

bands; massive and fine-raissed sandstones; loose black shale;; gray qussrtzose sandstones;velluwish-browis and greenish shales with thin sandstone bands; and grey qnarIese sand-stones. There are two main coal seams.

r ¡h 1,(!!(1r ihr (Jc/gr )r

Ci r pusss an agccgatr thicknrs o no ics tisati 40! rtrt They

cc' ii ¿uit coitad w i ib tite Lufeng Ser ics both on t he east t u i:' cci

ir rp souih, :15ev arc thrusted over ii' Sinht 1 roeLa' . Ois the lirtlIr : sidr.

tise ipinglang Coal Series r1SS gradually and ilnperccpLihty with nu sharpci ¿rnircation jEito the Lufeng Series proper by a succession of transrt,)nit beds

s.hos yo aciers in thickness. C. C. Young ann myself havc studiri Liese

hc'lc just riaL of Sbhtsc2 . There are yellowish-brown and e1Iowish-grccn shafts

nd sandstones which slowly give way to dark red and dull purplish shaly bedswith baril sandstone bands from the coal series upward to the stratigraphicallybiaiser and main dull purplish beds of the Lufeng Series. This observation isin contrast with that made by Saurin svlio considers the Ipinglang Cual Seriesto be snoulded oit an anticlinal arch of tiic LUfeng Series and equivalent t the

Sisilimen Series which he regards as the lateral facies of the coal-bearing strata

.iG.j .

Numcrou forms uf plant remains have been collected by \Vang andparty from le fpiigianr; Co-ml Series, but they have not been cxairiiued by anycompetent pacobotanist. The tentative determinations are not reliable and wifl

not be given here. So far the available data on the flora of the coal series otics regioli arc those given by Sauna (see p. 164). He considers this flora wbr of Rhactic age, but Coggin Brown who correlated his Ynanani flora withthis one regards it as of None age (see p.164 ). For the present, we may saythat by relying on the determination of the more characteristic fauna of thettcecding Lufeng Series, the Ipinglang Coal Series cannot be younger fian

Upper Triassic (Keuper).

Ueuaa TRIASSIC LUFENG SERLa5.Thc different beds of the Lufeug Seriesare completely exposed northeast of the Lufeng walled-city. Fig. 3 is a detailedgeologic map of this small area in which are located the fossiliferous sItes

that bear abundant Saurischian and primitive Mammalian rcmins

1. asi and t!arty regard these rock a-t 5br Sinian cr inetamorphmsrd marine Fi ias-i.

ViuF EHG

I EPLANiflo-

:Ø[h

/( - I XRZTAC\ )'f Ii -- - J2 1'.0 .. LdJpp h1-\fI t T brvtc'e-f \\ i '-XL '--, -' ''/ '.-' ' - ' 7 » es -/ - / \ ) , JPP 1MSCq

I/y I --' u1 \\ \ tU , i T'J j \, ¡ _,jb*7dj ñ ¿, 7?/:i,,j j -

4

A'?fl5

.

l5m.

/ t / J/ / \A1 U!4 3 -'

Jig. 3,Detailed ge Iogi Deip ot the fsiliferu area iiIhetst

twit 1*4! -

54tDcF/1o,S1 rr'ltj

Geo bciMøry

roei,t& 4ik. Wosetco,c4À w.tit n; c

0fltO&t20 t.cte-s

(Dat«p S4. /6hef)TGpo'ph bseJ

Poflof the. 'r'linfl(m5vcrvey

the I uletig it

Nus, 2-4] i3icn:'Rcd 1hd öf ?ti'tu 171

] (;z'o'usst t» ¡I

o( bcd irr a dsccuditsg ordcr is givcri as Ltl1uw:: -

I tCst JÁt!esg Scries ¡ir

Wiirr-rtd bruis. Bright nine-red clays, sisales and earrdseunez in alternatiur'

Occasionally with purplish earthy limestone beds. With rock tait, brine

and gypsum at Yuanvungching N of Ipinglang .

Varittgstsd beds. Pus ply, mauve, greenish, yellowish-green and pinkish um budawith strongly indurated limystnny bands in pinkish beds toward the upperpart and two dull purplish limy beds which display honeycomb weathering

at the lower third. Lower beds with greenish streaks and mottlissgs.4th and 3rd fossiliferous beds with ostracuds, pelecypods, fishes and turneroccur in this minor series ........................ I ¿It

1. ezisish-yeliow bauded beds. Dark tad Sisales and ripple marked siltetones withregular and pronounced greenish-yellow shaly bands toward the upper portion 70

lid sandtnne ........ 5-10

Lo wer Lufeng Series

1)urk red beds. predoninantly dark red clays, shafts, etitetoises and andstunes

in alternation. With two subordinate layers of dull purplish elements. 2nd

fossiliferous bed occurs nearly iii the middle part of this minor series or

about 70 su above the massive green sandstone. Rich in Saurisehise

1, Massive green sandstone. With occasional angular fragnsessts cil old rocks. Occurs

and quartz derived trous Siniars rocks ..................2as the upper or second breccia at Yaochan with components of quartzite

fluO purplish beds. I'redoniinaotiy dull purplish clays, shaiys, si!talouc and

sandstoue in alternation, while dark red elements occasionally occur its tile

fluOns bulk of tise series. Nearly stenly spaced green and greenish-yellow

tandsiotse banks decur near tise base. ist fossiliferous bed occurs at level

boat 300 su below the snassiye green sandstone or about 200 su above the

basal breccia Rich ils Saurischian remains. Fossiliferous bcds with

characteristic nodular or knobby ("Knollen") calcareous conCretiOOs.

Tubular ceucretions occur in loner beds. Calcite slates and greenish veins,550

treak or nsottlings crthing the beds in several ptanes are not uncommOn

luitl breeds Componeists of breccia are nsainly fragments of phyllite

[.ttrrdiattly derived from the underlying upturned Sinian ocks. At

Yaohan, the components are mainly q'tartzite and q.ssrtz ...............

Thc rvhu[c yenes has ata aggregate thickness of t,000 meters or usure. The

Sr ay th nr[e tevts 'ith a sharp uacfctrmiry uenn se ercty tjldCri S[nian

ti tite cut rit nil .ottbertt r riic Lu et. [U

j ti the Ipinglang region, espeeial1 e.t of Sht e, tii .iull uttri1 ;h hed of theseries o ;crlie the Ipitsgian Co-al Sert-s cotiïori-tbt y without a ny basal breeci

but with a series o transi' ion-ti lClt ineuttonerl itt the previous sCctOii.

Fault contacts between this series aoci older rocks are quitt commou. Tb'faults often cut the lower horL'otis of the series out of view, cg. north oIE

Shihtsengtze' only the Lipper Lufuiz Series starting frotis the greenish-yellowhanded beds are epusel.

Saurio made a study of the petrographic ch tracters of the series and alsothe overlying Shihmen Serics. According to him the constant presence ofraititic and detrital tourmaline elements, which are little worn, throughout tIte

whole series seem to indic ste th mitts source of material was derived throuhthe Itrocess of a slow aoci prolots'tel erostoti in place of a granitie and metaumi.rphic

region 124, p. 456-457).

Fossils, especially Saurischian remains, are quite abundant in this series.A complete list of fossils so far determined2 and assigned to their respectivehuri7.ons (seC Fig. 3) may be given as follows:-

Upper F!yo1ue- and T5nionitl-beariti t.ufetg Seties

4th fossiliferous bed

(tst tacad e

Pelecypods

t Tnjonids

3rd Insulterons bed

Oetr?cods

Pekcypods

tin ¡on î ils

Pisces

Ganid fich 'cale-

hosiiiette,sis 'ottne (at Yr,ocltan

Reptilli

t heloit a ¡ niet.

\lnsst of the f -ei collectes! save beets kiel is studied by t'.. t . Vnst,t,', Foi hts.iie2t itt irin, t lie seadtr ¡s efet t c in hj ot ¡ital ÇS-42)

1. 2 Ul: 3. trt; 4 » 5

171 ïJu?etin 0/ t!ss Ger'!ogicui Soiit'iy o; C 1»

E nwer Carnusauria and Be,:ot1iecir,sn -bsaring T gifeiig Ser les

2nd fossiliferous bed (J-TuarEiatitn' and Erhrbuarsshar sises

Re ptilia

Pseudosuchia indet.

Saurisehia

L,ikotisausus )i)5 Young

Sinosaurrss Í5iessicus Young

Gjposawiii sinensi.c Young

Y,iznanosaoros Jinangi Yosmg

Lnfeagosaurus hnessei Young (precence qitestionahle)

Lufengosascrtsc niagnill Young

Probable presence of a true Pi-osaurotuid reseinls1in

Plat-go

Tlanima1ia

?Triconodonta badet.

Ist fotsi1ierous bed (TacTs gagS and Sliawsn sites)

Reptilia

Saurischia

Lukotgtatsrus yini Young

Yac nanosatfrus ltuaagi Young

Sino caucus triassicits Young

Gyposaurus si,jsnth Yonng (also present at Yaothan nd It, busof Ipinglang)

Lujengosjuiriis h is end Young

Liifengosaurus mag nus Young (also present at Tatao1sing in sheIpinglang region)

Mamnialia

Tritylodontoidea

Bicnotheriuni yrsnnanensc Young

Bieno/heritim ciegan, Young

From the 1it of fossils given above, one can see that the ist and andfoscili frrous beds though separated from each other by no less than oo meters

No!. 2-41 Bedi of Yiuimu

of relatively non-fossiliferous beds bear essentially similar faunal as5eI!i

The contained fossils definitely indicaic an Upper Triassic (Keuper) age for tueLower Lufeng Serics. Fossils from the Upper Lufen Series, though less

characteristic, can still he considered ro indicate a Keuper age, but by noas certain as that for the Lower Lufeng Series.

Although most of the Saurisehian and primitive Mammalian remains aredscrihed as new genera, if not new families, yet they show extremelY clo5

affinities to similar forms occurring in the Red Beds and the Cave Sandsi (flCof the Stor,nherg Series which form the uppermost strata of the famous ESsstivi of South Africa 8), or those in the ''Knolleninergel'' of the GermanTrias. Young's reference of one of the Prosauropod species to th South

African genus Gyposaurus is significant.

Up to the present no exact equivalents of the Lufeng Series hove beenrecogoized outside of Yunnan. The "upper zone" of the Triassic beds of theLiaohsien-Yushê' area in Shansi with a Theromorpha fauna (Sinoka,acmeY1Jpearsoni Young and Dicynodontia indet.) is considered to be Upper Triassic f32,3), but it cannot be considered as an exact equivalent of the Lufeng Series

?JURA-CRETACEOTJS Sr-iIHMEN Saaias,This series is extensively exposedin the Lufeng Area. It possesses a basal cnnglomerate of varying coarsenessthat ranges from lenticular pebble conglomerate to macN'e boulder cotand lies clisconformably over the LuEerj Series. Tise components arc nIa 01V

quartz, quartzite, some crystalline limestone and phvliitc. These are derivedfrom the Sinian beds. The conglomerate passes upward into mass-iVC dull

purplish-brown sandstones. These sandstones are current-croscbedded and graduallygive way to banded sandstones with evenly spaced shaly intercalations toWard

the top of the series. Its thickness ranges from xoo to 300 meters.

I-Iitherto no fossils have been found from this series, By its stratigraphieposition, it is tentatively regarded as of Jura-Cretaceous age. The possibilityof an Early Tertiary age has been ruled out by its structural disposition. The

Early Tertiary sediments so far recognized in Yunnan are limited to separatebasins 2], while the Slsibrnen Series is widely distributed and flvo1V1 il

various types of structure.

1. m±

1 foutu uf tic Geu1oii oejc1 y

3. Cioui:

Pi,to-Ii.eisiocea CAVEi.S AMI) 5 Nos.The rounded lulls which arcullied in the northern portion of the Lufeng walled-city itself and around

Husngtupo' are composed of a series aL horizontally disposed gravels and sands.The gravels it the hase are well sorted and sometimes slightly indurated.Folloviiag the gravels, there is a series oL pink and reddish sands with occasionalgravelly lenses and clay loamso Iron pans also occur in the clay looms whichare frequently mottled with whitish streaks. The sediments seem to be of auvialor fluvio-lacustrine origin subseuently attacked by a soil-forming process rhatmottled the clay looms and formed the iron pans. The estimated thicknesc of

this reries is over 40 meters.

A nother outcrop of sands with two poor lignite seams occurs at

Hooch aying northwest of Chungtsun3 may be regarded as contemporaneous

deposits.

The patches of mottled red barns without bedding (not shown on themap, Pl. II) occuring over the Shihmen Series between Yaochan and Lufengregarded as eolian loess by Saurio f24, p. 465 seem to be soils formed on theShihrnen sandstones by the saine soiJ-forming process that rendered the claylooms around Huangtupo mottled, though they occur at different altitudes.

The three deposits mentioned are all without fossils. They are tentativelyregarded as of Plio-Pleistocene age.

QUATERNARY DEP05ITS.The recent river alluvium covering the Chungtsuaaoci Lufeng plains which are separated from each other by a hardrock harrierformer! of Sinian rocks near Shihhuipa4 in which the present Peiho5 has cut ashort stretch o gorge.

B. Structur.

An inspection of the map (Pl. IL). and the block diagram (Fig. a)reveals the fact that the Lufeng Area is affected by a series of high-anglefaults which generally trend NNE-SSW. In the Ipinglang region, these faultshave cut short the NW-SE or E-W trending overthrust fauhs of small throwthat effected the lpingla'ng Coal Series only.

1. 2 3. ii 4. ffJ; .

05. 'i4 - 1 J-Je of tiO!?J0 1,4

Ce couilt e rue h eli-wele Í,ilts. the Sinian ruek.c as weil as tb'Tpineaii: Coil Series are hrt out as structurai ridges or horsts. Thehounding faults ai these horsts a re u varying intensity.

The fault west of Tachung to the north of Lufeng is one which diesour within a short distance north ward and grades into a monoclinal flexor':

southward (see also Fig.

West nf Hsschiachang' to the south of Lufeng, there is a fault whichhas cut oí a portion of the Lower Lufeng Series. Moreover, it has intense])aíected the beds immediately east of it where overfolds and vertical dips in theLufeng Series are observed (see aiso f. 3 o Pl. I), hut they progressive]\'and rapidly decrease in intensity toward the east.

North of Hsiushuikou' , there is a small tear fault that trends E-W. Asmall low-angie thrust fault that strikes NE-SW occurs within the Lufeng Serieswest of Vaachan.

Disregarding the peripheries, the extensive heart-shaped region of the

Lufeng and the Shihmen Series is on the whole but mildly flexured into a flitsvncline, The axis of which trends NtE-SSW.

The bounding faults ois the western front of the horst of Sinian rocksare very intensive in nature. At places, they have faulted the whole LowerLufeng Series out of view. This means a sratigraphic throw of at least 700meters. The intensity is further expressed in the isoclinal fold involving boththe Lufeng and the Shihnien Series irrimediately adjacent to the bounding fauit.Here, again the intensity decreases progressively and rapidly when passing awayfroua the faults, because tiiC isoclinal syncline gives way to an asymmetricalanticflne which in turn passes into an open and gentle syncline toward the %vest.The axes of these structures trend nearly north-south.

lt is quite clear that Credner's cotitention of separating the 'Red Beds'into an ''elder folded Red Beds' and a younger ''flat laying Red Bed formation"on structural ground is untenable. In fact what he regards as the ''elderfolded Red flds'' are actually tIse younger part of the Lufeng Series.

From the various cvidncs given above, one could gather dutt, with

the exception of the minor thrust faults limited to the Ipinglang Coal Series,

t. T*.. . 3*i.

fr; [lie C [Vii. XXI,

fauhing and folding ire mutially rrl.sed and therefore interdependent and

contemporaneous. Moreover, it may be interpreted that they are the expressionscf crustal relief of a regional eastwest directed tangential compressive stress.

The dating of the periods of major deformation cannot be accurately

determined in the Lufeng Area, because of the great stratigraphic gaps.

Generally speaking, the Sinian strata might have suered several periods of

deformation before the deposition of the Lnfeng Series. The unconformitybetween them represents the movement or nmvements that happened after the

Sinian and before the Upper Triassic. The faulting and its interdependent

folding represent another period of major deformation that is post-Shihnicn

Series and pre PlioPleistocene gravels and sands, because the latter and later

materials a re undisturberl.

The topographic expression of tue horst of Sirmian rocks is that of arelatively low area, while the Lufeng and the Shihmen Series on its boundingsides stand out as higher regions. The massive sandstones of the Shihmnen

Series form prominent escarpments or cuestas when dipping gently. When

otherwise, they are reflected in the topography as sharp and distinct ridges.

Most of the interfiuvial upland surface of this area is one of matureconfiguration, while the vahees dissecting it are of youthful stage. Inasmuch

as the master streams in this area have lodged their courses in gorges rgardlcssof the conliguration of their underlying structure, the suggestion of their beingeither of superimposed or of antecedent draivage immediately come.s to one'smind. Owing to the complete lock of evidenie to support superimpositionantecedence seems to be more plausible. This, of course, inlies the existenceof the essential drainage in this area antedates the post-Shihtne deformation.No definite statement can be made beyond this rather vague conclusion, becauseof the tenuous nature of the evidence.

THE ANNINO BASIN

Fig. e gives the location of the Annina Pasin. A general impressionof the topographic and structural exoressions could he gleaned from an inspectionof the uild sketches (Fig. 4). the diamam (Fie. ç), and the emalogic

map (Pl Il Fl nf this basin.

I

<ur

nvkh

nlc

nshc

ui1h

Tht

C&

.---

--'..

.p1;

- u.

-.

Pkiii

sIan

çT

t.siu

eeor

otoc

.

--.

----

--...

:-.

----

-.-:

UI)

PÑFh

ö.n

(5i)

shu.

puPw

y

-

Fig.

4.A

. Loo

king

soo

thw

est t

roo

Shsh

au.

B.

Nor

thos

tern

coi

ner

oth

e A

nni

Eaí

in v

icw

ed f

rozu

Ch.

knog

s1ia

n.

The stratigraphy of the Paleozic rocks in the environs of Etusining have been repeatedlyinvestigated by T. V. Hsu, C. S. Pien, H. C. Wang, T. C. Tseng and others, For details theeader is referred to the different papers writt5n by the various al,ovc-mentioned authors (t14, 27 and 23J.

According to Y. I-I. Lt (personal coonnunication)., the two smaller strips of outcropsniarked (FI) as Sirias inst seuils at Hueiwan (jii) on the map (Pl. 1(1) are actually LowerCambrian liinestones. The structure thtre is a repetition of the tower horizons of Lower Cambrianrckr, which means that the thrust fault shown should b shifted westward to the line betweent In stripe marked (H) and she repeated cuver Cambrian siales and sandstones. This change alsi

w t:e blwk diagr,nm (Eig. . Tie lsrCcc stip niarked ill) notth of Nrianyinsí iThH is correct.

-k L Ill.

Bit/f o! «/!, Iv0!, xxr,

A. Stratirapby

I.

Sf.\N..Rocks of this age are extensively developed to the iorth (t tIseregion under conakieration. The relatively younger portion observed comprisesof purple phyllites, thick series of conglomerates; white quartzite and bandedlimestones which are siliceous or otherwise. No estienatiols of the total thicknesshas been made.

Lowea CsaruAN..Following the Sioiati limestone conformably is a

reries of arkosic sandstone, black chales, alternations of pink or yellow fioe

grimed sandstones and yellowish or yellowish-green micaceous shales (fossiliferous),and occasionullv followed ty a thin bd of limestone with dark stripesa . itsthickness is around too meters.

Specimens of Rcdiic/iiz C12J00O515 Walcott and Oboius' chinensis Walcottwere obtained from the yellowish-micaceons skates at Chikungshan3 where theLower Cambrian beds and their ttormalty overlying Paleozoic rocks are completelyoverturned on account of overthrusting.

LoWER C.RBot'uPERous.The rocks are composed mainly of greyish-whiteliniestones intercalated with characteristic pink litnestones, shaty limestones,purplish skates, and bauxitic shales which occasionally intercalate thin coal seams.They follow the Lower Cambrian rocks disconforniably and their thickness is

about coo meters.

ANTUACoLITUIC. The Permo-Carboniferous rocks are mainly composeelol massive limestones with intraformational breccias. Their color ranges front

- L

iiie;i:''Rco' JJcd' oj' uriouo 181

v0ite to dark grey .Ace ordin; LO the studies oi lisU, Fiei a'ol l;ci', L

7]. they comprise of i-luangiujl4, Maping. Cuhsia and Miukou liu)tO11ci.-ait of the Chihsia aol most ut the Maoou li:nestones asinine a patchy

appcarancc oti account ot dark clavish inclusions. '1i'aggrcgat. thickn:s o:

he Anthracoljthic rocks ranges from 700 to Soo meters.

iJt Pansii. --Following iivariably the Maokou limestone coistor,nahlvis ioup of igneous rocks which should appropriately be called a volcani e

serier. This series is composed mainly of basaltic flows with inclusions of 1argangul4r blocks and smaller fragments of limestone in the lower part. The

uppermost part may sometimes be represented by purplish volcanic tuff or

t1ifla;u,,ui shales, The estimated thickness varies from ioo to 150 meters.

The volcanic series is usually correlated with the Omeishan basaltThe question of whether it is of submarine or continental origin has not been

hitherto settled. Evidences gathered recently seem to favor both hypoiliese.

Beyond the apparent general conclusion that both types might have occurredsiïiultammcously, no definite statement can he made.

Finally it should be uoted that the Palcozoic formations follow each otherin apparent conformity. No angular discordance could readily be detected

between them right in the field.

2. MEsozoic

Upi'eii TzmAssmc LIJFENG SemuLs.Overlying either the basalt or tulfaccous

shales nf the Upper Permian volcanic series disconformablv, the Lufeng Scrielenmnsences with a basal conglomerate of varying thickness that ranges froni a

meters (SW of Chihchiapi1 ) to au meter or inure (NW of Taihuassu ) - The

components of the conglomerate also vary from place to place, but they are

nmstly well-rounded. Limestone ciemnemmts in pebble size predominate, whilequartz amid quartzitc elements which m.ty sometimes occur in boulder size conic

iozt. l3asalL pebbles arc extmaordinarily rare and usually occur isear the base.

huuli basaltic elements might h:t';e imide up a large proportion of the rather.

coarse matrix.

Following the conglomerate, there are alternating beds of yellowish-green

audsiones, dull purplish, aoci dark red sisales. Then there i a massive green

1.KT ;r,/?ii,i ,J ')t'-tCf S 'if 4t 10f!

sandstoiic bed with purple clay lab lite usions which is in turn folluwe I be Juilurplih sIles. 'fleo thickness of thsc beds is 2)0 meters or mo. ïhey are

regarded as the Lower Lufeig Series of this basin, This es mainly based ute

their litholugic characters, because no tussils have so far been found.

1 hc Uuper Lufcng Series saistiug of pinkish sandstones, reenish-yellow banded, variegated and wenc-red beds ic very well-developed in the AnisingBasin. The aggregate thickness is no less lIsait r,ouo meters. 'There arc sottieminor differences irs lithologic characters as compared to the standard LucngSection, cg., the occurrence of more massive sandstone banks ire the wine-redbeds, arid the presence of three constant purplish earthy limestone beds near thetop of the same beds. Sonse brine wells are sunk ije the wine-red beds bothin and outside the northern part of the Anning walledcity.

Fossils obtained froue thc Upper Lufeng Series are as follows:.

(I) sp. indet. aff. d ltt'Çt Quenstedt to a sajidsto,ie rear l,a,e ufgreenish-yellow banded beds SW of Chihchiapi.

E1!jcia -, ECtíthria sailli Masuy and ostracode from greenisli-yefluw handedbeds at 19 kilorneter-niark fron Kunming along the Yunnan-L'rnsa l-Iip!5ynorthern portion of Chikungehan; and road-cut usar SW ofAnalog,

¡Iybodrra horrticne,;ei,s Yocn: aid traces ut Chelorils frote variegated beds ease niKoutiun1 ; several forms of Uniouirls. gemid fish scales, osirsvd1, and enenitiute pelecypods and gastropods Iron rai isgated beds at east of 1-Ionen andnear Tatuanshautsuri,

'I he faunal assemblage is essentially similar to that of the Upper Lufc-ngSeries of the Lufcng Area. A regional correlation of this series between the tworegions is affected by the common presence of the foasil shark Hybodshoutieiscnsis Youtsg.

JuRA-CseETAeaous SHefesaoN Seivas.This series is represented by massivecurrent-erossbeddcd sandstones of dull purplish-brown .colo which gradually passinto banded sandstones witte regular shaly intercalations. Its thickness is encrethan roo meters. Notwithstanding the conspicuous absence of basal conglomerates,the lithology is essentially the same as that of the Lufeng Area and is consideredto be overlying the Lufeng Series disconiormably.

1, !lflIi'; 2. )l1.

No,, 24) Bit'n :-' 'Red I$cds'' of 'i'un nan 18$

3. CENOZOIC

1to-i'LILlsrocExE ucossi's.()verlyiug a somewhat channeled uIaethat truncates the tilted beds of the J cug Series about So nieters above thapresent flood-plain, there is a series of gravels, yellow sands and ycl!osvislibrossbarns, It forms a vehl-graded depositional uface. The thickness of this scri.svaries from 5 to 15 meters.

At relatively lower leseIs, some gravels with bands of pinkish, ycilowisis

and greenish sands which arc also undisturbed were obscrved at certain loaliiicsin the Anning Basin.

SQuth of Chinshauching' , there occurs a somewhat eroded talus depositwhich consists of boulders of considerable size composed mainly of Sinianconglomerates.

The three deposits mentioned above ar am non-fossiliferous and theyare tentatively regarded as of Plio-Pleistocene age.

QuATzRNMY aposirs.R ver alluvium occurring along present streamcourses except at rock barriers composed ut Upper Permian basaltic series

surrounding the Anning Basin where the streams have cut gorges across them,Shihlungpa2 is an example of this, where the sudden change of stream gradientof the Tanglangtsuan made it a favorable location for the hydraulic power plant.The red residual (?) clay deposits occurring in some small interinontane basinschiefly situated jo limestone terrain also corne under this heading.

B. Structure

By an inspection of the map (Pl. Ill) and the block diagram (Fig. )

ut the Anning Basin, one cannot fail to b impressed by the arcuate effect iii

structural pattern exhibi2ed by the Paleozoic rocks flanking the infolded Mesozoicstrata on the north and the east.

On the northern border of the Auning Basin, outcrops of Paleozoic rockscomposing the LaochinshatsZ and Lungmashan form an arc with the concaveside to the north, one end at Chincrhssu on the northeastern corner of thebasin and the other at the mountain known as Pichiashan5 north of\Venchuantsun7 . Coursing inward from both ends, where the Palcozoic rocks dip

:t 4 /rt//çIiíi of iL'c Gco1oisi1 oc,çtï of C/;iov

3 4.

Øj 3, t. 4flj

L rl; 2 i«; 3 1. 4iù(Vqil): S. UL 6'

2-41 Ii!-n:__'Red Reh'' of Yetno

basin-'vard or a1most vertical. there is a marked swing with simutane01Irroving in horizontal width uf the sarns outcrops hot the Sinian toward the

frontal portion of the arc until nearing Chinshariching where they dsapgeare mass of Sinian rocks which override the Upper Triassic Lufene hed

direetic Coincident with the progressive change in strike, the beds bee.neoverturned coward the convex side of the arc, leaning at lower and lower angleurn il thee are recumbent, and incidentally breaking forth into an overthrustfauit which is of low-angie at the frontal part. Chikungshaa w-th its completelyoverturned Paleozoic sediments is in reality the most southerly frontal lobe of

hc main thrust block of Laochinshan being severed and isolated fron the latterby the northeasterly trending high-angle reverse fault northwest of it, It is a

thrust oudier let dowis by the reverse fault behind it in regard to the thrustplane (see Fig. 5).

This observation greatly dijiers from that of Saurio who considers the

structure of Chikungshao as a buried anticline 1,24, p. 451 and fig. ). Trie

rlace-nme 'Tzu Men Lu'' used b him is reiht' Tzemenk , a village on thesouthwest of Tushupu'.

There are two tear faults associated with the main thrust fault, one northof Fangmaitag' nd another rust east of Chinshanching.

On the eastern side of the basin, the Pichishan (Sishin) and Tachinshartsrem to form the western wing of a mach compressed arcuate structure with iSconvexity pointing southward and the eastern wing lost in the Tienchib, but ithas to be said that there is no proof to support the previous existence of aneastern wing. Starring from the north er Pichikuan', where the Upper Pernalaribas&lt is slightly overturned basin-ward and dips strongly to the east, there is 3remarkable twist in the contact plane of the basalt md its overlying conglomerateof the- Lufeng Series to basin-ward dip when going southward. This basin-warddip reaches the amount of 400 at a place northwest of Taihuassu. Furthersouthward, the Paleozoic rocks again tend to overturn toward the cnnve sideof th arcuate curve, inclining against the sympathetically upturned or oveifoldedLuir-u0 beds with a pro.,ressive decrease in intensity of dip down to recumbency

01 ii;? of

I in 1h rctiiaiit it» it the I 5V-L V n.-tciirnt colt i01iij ij LtsudLtt1\YCat of Kna nyinslian '»'bete C irhon ícr»u rocks are bruught i tito Wrect ntacts ith the Lufoug lods.

}-Tigh-angle clear thrusts occu r iii tice houndarv zone between the basaltand the J:ufeng beds. The le rgest one occurs east of Paoshan' and a smalir rl'oc floitheOSt «f Kuaniang2 Both trend nearly north-south.

There ts also a high-angie shear thrust involving oniy the Lower Cambrianrcckc ( '»PC flOt-nOV 00 [1. 1Ro) thor rends north-south on the inner side of titeaccione cf ucd ore just described and citiiat.el on the east of Tchinchn and rouchri TJcicit'»in.

Te cauchet ti louniarv of she ludo is not dii' ted by ovcrfolt1in ertilt 1SIiti, it it itocin wad 'lips tif tv l'O5i i-ds 01 the I..tiÍn Ir»riec sr-

o:casïotiiiii' qtdc» t-ep. A high-angle clic-or thrust of scnill dimen'jcn chatt vols cnotilv ran-west occurs in the eastern port ion of TsaiCngsha n

Tin- .cr»: soi.iW 01 Lcinshau4 on the northwestern corner of the basinwhich is inferred after a hasty rec000ai.ssanae in the Tsaopu and Pin:-;tishao

regime ivill not be described,

The Lufeng beds, especially those on the northern and eastern peripheriesor the synclinal basin, show marked sympathetic upturning anti overfoldiug seitl.

their bounding structures. As in the Luieteg Area, there is again a noticeabletendency of progressive aced rapid decrease in intensity of dip of these lethtowards the center of the basin from its boundaries.

A miccir flexure in the Upper Lufetcg variegated beds wit-h northe;isierlvtrend occurs to the south of Chikungshan.

'lite outcrops of the Jura-Cretacerus Shihnoeñ Series composing thePingrinesh in aoci Ilimishan8 show a general outline which somewhat agreeswith that of die main basin and clip from 15 to an degrees inward in accord mccwith the Lufeng beds directly underlying them.

Notwithstanlin the fact that tise structurai trends may strike at rightnglec. ta e.ah oth'»r, yet it is quite clear that folding. thrusting and cross--

are ittutualiv related anti theretote interdep:ndent and contcmpir0000uc.

t. W itt ; .. Yf . 1, U lt . t t- JtI

1' T » ftf l-»t ft.

r 7-4! 141'---'P'J t

-lru'I'V piakitu, over tudoig, hc fl;c vcI;muiin .01! o

javr nr'ccded tite high-anlc reverso md 'it.-r faultin The hur.Ï v me

nf crustal relief for 111e maiu compressive force oh ti ib tattcbeing time results of upward mnigiation ni exce's material caused b" the sei cre

niarginal bending of the svn;,line attendant upon time lutiner furces. 1 loses r

vhen viewing all the diverse structural element s as a whole, it is i ncreasingi':

clear that they are the recipocai adjustments for the relief of a simile cV-t COi

of pressures resulted from a main southerly dkectcd compressive tanzotia1 stressJo short, they are cogenetic structural ciernen is.

In chronology, the structures described above must hase been caused byan orogenic movement that happened after the deposition nf mlm Slulmim'meri eiiea

and before the undisturbed Plio-Picistocene and later materials Aside front thisratier broad conclusion, no definite stateoant cart he given.

The topographic expressioms of the main structures here is quite straight-forward, l.ecause the structural synclinal basin is at the same time a topographicbasin. Upturned strata, especially the Anthracolithic imestones, are reflected

in the topography as nearly symmetrical hoghacks. The Lungmashan andTachinshan are good examples of this type of erosion ridges which assume aloilgitudinally striped appearance. Changes of strike in the basin are expressedin roughly crescent-shapcd ridges, such as the Wukungshan' which is concavetow's r is the center of the basin.

The great scarp of Taoshihtou2 which is well-known to most of thevisitors of Kuriming seems to be the result of erosion upon steeply j nelimiel

joint-planes of the limestones composing it. It is true that some investigatorsdo look upon it as a fault-line scarp or even as ass obsequermt fault-line scarpwhen attempting to explain the origi.n of the lake known as Tienchih. Prescutknowledge cn this subject, however, ducs not warrant any dfinitr statement,

Upland surface surrounding the basin, especial!' he Lau hine!:an naseS,shows nature configuration. Tise streams draining the basin 1mucv 'pnilm iii

characters at stretches. Tnglangtsuan, the master strca ma that rIrai mis lit:Tienchih and crosses this basin no its 'vay northward to join the I 'ppr Ya nptsto,shows. a marked lack of reflection and adj ustmnent to its underlvin struct nie.

1. I ¡li . 2. (j

1, 2, 3, Ø*4.

1:: 1;//pjjt oJ !! I Sota-i uJ ('j:/«' -

TI-lE SHESIIAN SYNCLIN$3

'1 lic stratirt'b and rictu of the hshan SYOCi inc v1iiclt is

&n tc north the Kun m g walled-city have been ably studied and dascrihelby l-1. C . \Va ng 28). T. Y, Usc aidm; self have also visited the SOO!it riportion of this syncliu. Hsu has already expressed the ina.Jvisabilit of a t

fold division ot the iRed Beth" involved in this svnc!ine rsJ, We see the

hds there as represeririug a part sf the Lufeng Series beginning from the ko"rbeds with several layers of un to the greenkh-yellow hand-ed bedsof the Upper Lufeng Series.

'[he structure of Shsl.sa ttelf is essentially a homologue of that of

Tachirishan on the eastern boundary of the Arming Basin and reflected in the

topography as a distinct hogback. There is also a repetition of the Upper

Permian basalt ad a small part of its overlying Lufeng Series by a shear directcaused by se ;ere marginal bending.

TilE SUNGJIUAPA BASIN

Sunghuapa1 is situated a-t about 15 kilometers to the northnotheast ofthe Kunming city. T. Y. Hsu has already mentioned about this basin ri hispaper on the geology of the Kunrning Environs t

. Lufeng Series up tovariegated beds is iuvolvd hi this severely inoide-;l basin surrounded practicallynn all sides by the Upper Permian basalt with strong marginal dips whclsshow progressive and rapid decrease in isuensity towards the center of the basin.Of structural intcrest,- it may be noted that to tha north of this basin at

Hueiliuwan2, Ordoviciai maki arc seen to override the Upper Prrmian basaltfrona the north.

TUE YANOLIN SYNCLINE

Yanglin is situated on the Yursnari-Kueichou Highway and also thepartially completed Suifu-Kunming Railway at about 6o kilotiieters northeast olKunming. The actual syncline is on the east of Yanglin that strikes tearly

northeast-southwest and has been studied by C. S. Pieu [22). The 'Red

Beds" involved in the aylal portion of this syncline are considered to he univa part of the Lufeng Series composed mainly of wine-red beds with a hit-kich

basal conglosnerate ruade up of pebblec of basalt, limestone, quartaite and aC4C.

They are underlain by Upper Pernaian basaltic series.

Nos ihcn:--- Red Beds'' oj uona,

TU E StiUITAN1 OVERTURNEL) SY NCUNE

Shutuig is a station on the Yunnan-lndo-Chini Rdwy hot 'yto the casisoutheast of Kumning. This overturned 'nine ha Ieen

describ by T. ' ¡-isu and C. S. Pje ' 3 It strikes nrj rwrthc.sctsouthwest and os erturus towards the northwest. The "Red Beds'' ,nvcdved n

this synclinc according to Hsu and Pien possess no less than layers of

congIømcte at places, followed by dull purplish sandstones, yellow coarse-grainerl3adsto1C, greenish-yellow banded beds, and a 40-meter siliceous limestone.

They are underlain by Upper Permian basalt.

Plant remains erst suspected to be Equisetites, now rccoguized to be

edinglY similar to the rhizome of Equise:uin areoaceuns of Keuper aspectdescribed by Nguyn-Ngoc-Chan from the "terrain rouge" of Eastern Tonkin

in ludo-Chiita were obtained from the greenish-banded beds by Hsu

and Pien.

The problem of whther the thick liinest,,oe is a lanral facies of thevariegated beds of the standard Lufeng Series, or an indication of its proxunity

to the Upper Triassic marine transgression from the south cannot he settled vet.

OTHER PARTS OF THE LAKE REGION

According to C. S. Pien2, there ae two roughly crescent-shaped sy uulin.ilbasins with Lufeng beds between linen and Kunyang5. The beds arc said tu

be lying unconforniably on different Paleozoic beds.

Southeast of Chinning', according to. C. H. \yng, there arc

Beds" involved in a syndic which overturns to the northwest op account o tue

vrhrusti1ig mass of Anthracolithic rocks frrrn the southeast which form th

Liangwaflgshafl. 'I have had only a very issty glimpse of due "Red Beds"

there and they seem to be represented by both the Lufeng and the Shihmen

Series. Whether all the different beds are present there still remains a prol-leis

to be ascertained by more careful field studies.

Around the Hosi' and Chuchi8 region, Y. L. Wang uÏIa)1)Cd

considerable area with exposures of ''Red Beds'' [29, pl. il which according

2. Personal comrnuniCtiOL1 3. Il 4. !; 5, P'rmal eon,-

t'. . : , «J ,

ii .i( ((0i'YiC(o/ I'Ii11

ii' i.rc .it n.' .iI:kc i1 litholc ji bc k lt til\Oi\d in k Annincn The, 'j.., ocriic ;tliracolishc 12 onee .ini strike e,,raiic

V

111E 11JMIN ûVERT1JiNt SYNCL1NE

P Lilo II c:t y s about 30 kilonicters to tue northwest cb Nition i't ( re

C. C. Yooip; and myself have studcd this inlerestilig CflCli0 W2hCt

r-erl oros to the outhwcst. lt is somewhat ar.uatc in outline with the :oncaetide facing sortheast and is situated on the wcst and southwest of ikoalied-city. This troctore invoket the \nthuaco1iciic limestoises , Upper Ucraitanbssalt, the Lufeng Series aol the Shihiteti Serie. The Lufetig Scries coininelti s

with a conglolnerats composed mcdnly of quarrahte. ivartz. sono linlettonc and

basalt ebbks. This is followed by dull purplish slides ud siltitoncs v.'hh

OciiUlSr caleas000s concretions, sorne variegated beds and t.heit tIse characteristic

avuiered bcdc, The Shihmcn crossbecided dull pue1di;h-brown sandstones again

witli.tut bisai conglomerate are folded into an isoclinal syncline that kaut

southwestward in accordance with the nain structure. On the northeastern

limb of the main syncline, Arithracolithic limestoncs and Upper Pcrniian basaltarc obervcd to be completely overturned.

FROM PUMIN TO YUANMO BY WAY OF WUTINU

_Noth of Fumm at Chaipai1 , the variegated and svinc-red beds o! th

topee Lufeug Sertes arc well dcvclopd and gcuerdly strike N3o°E. At Mati

Li\VCCII r:haipai and \Vuting , the lufcng beds arc seco to be overridden bylimestones from the eastuortheast somewhat in accordance with

K. Krcjci-Grafs observation (see p. ifs).At Wuting, the Lufeng ant Shibnien Series arc seen to dip at 20 dcgrecs

ni more northwestward with Shihrnen sandstones forming prominent escarpment..

1OIIt Writing to Yo-aonio, the route lies most of the way on gentlynnbl_ii nc Slsiicmcii saudtfoncs which a surface of rather mature aspee!.

.\r Ysarinin. the Lufeng beds underlying the Shihmen sa ndstoncs yielded

;lO,ïcI lich calcs dniilar to those found from the variegated bols of the Lufeig

ras son the Anning hasin r, p.

1.

2 4 I 191

tiOi\ \'UÀNr1O TO t tiF ,N(j liY WAV OF VI2NIiS(N(j

hei svr:n ï Uenrve:oi'IC.it eser' h

L.rg erics thu strilz OCItÍ c;twcs. to be iitg w;th O 1(M!jtfl t

ou a series of. hiçhiy euni:oried greeisisil s:ii1si wItih tic g t netIcuau:;

entaut with a rather lai ge intrusi e grutiiic body i tug to the .1

nieta niorphused greenish sb:dcs arc of probable Plcoioic a ge

fhis observation so I \vha t arecs \vltit that made n'

the 1ungen regIon in the tact lhtt neither tite Lohnt; Secier luir it underlying

11'iugiang Coal Series are aflc.ted by the rafli1C inirUSiOJl nf nertherti luinart

in a north-south tract lying roughly treulli tIte 02 id meu iditu.

From Yenhsing to Lufcn via the sturoduiiig rctioui OO\j,

ï uanyuugehing, there aie pr:tCtiC.t[lY oti1itio0Us e: jures Uf ib.: liticrrur. b.k of

tise Lifcng and Shibrueti Seiie strlIiitig generally north-south ant tIti.i'211 folded.

O'l.IlL} OBStVATIONS

The distribtttioi and gucral cht racterictics ut tb; Lcd icds \vtt eand Southwestern Yunuan have been ve1l sunsined up by t_.ettgiu tirona [ ,

and pl. 30 ). In the stretch between Lufeng and Vunuani, both the Lufeiig and

the Shihnsen Series seem to be present and folded together. This observaijots s

based upon several personal reconnaissances of rather a hasty nature of mine

between Lufeng and Tau. 'rhe "Red Beds" at, Tsuhsiung' SCCIIS to foini a

synclinal basin.

0E intercst, it mtv hu n tcd that in \Vetcrn Yuunan , especitily tu tite

region from Hsiaugyun northward pass Pingtsuan up to Yungshcng7 whete

the Upper Permian basaltic lava again flourishes in exposures as in icastern

Yunnan after a bari'en asedian tract lying roughlu betwccrs the soi st ant tb:

102nd meridians, the basalt does not diic:tiv underlie the "Red Beds' as

around Kunming. Instead, there are Upper Triassic marine beds of limestone

and shale, and a coal series of the Ipinglang aspect between them without any

angular discordances. The most up-to-datc observation of this true of relationship

is tb-it of K. L. Fang and W. K. Kuo in the Yungshcilg area [ 1 though the

"Red Beds' have bcn regarded as of Cretaceous age, vet they hive been cotrelated

with the Luferrg Series on the basis of lithologic stratigraphy.

U' (j 4i '3H I-iutI F,]!iI'5t0u t I . ï

Ac Itit.

192 fl4i1 Qt r' u.

r!j'ip th,t occurs at Mengisua o- i;_ 'juh nl dv. irr Iu

O5C! ld S S' 'rtov 1) be nentoned. li W,S iserVd by C. d, 1 .n -vid

cj, pi. il. ' here We see a series of 'Red In1s' intruded b'; cr.csa od oiiÇorntabiy overlie coal series o the ipingiao 'spe;i which in turn dunderlain by a series of thin-hedded limestones ain diames that bear H'i'n

Jropi'i,z napengensis Healef Although T K. Finaug has rdised th'. Red Beds'' to Crciaceous when he edited the paper. T stwngiy (ret

that they aie the l.ufcng Series, because the' toilow the coat series ot tl1

Ipinglang aspect in the same way as those in the adjoining regions and aiothe Luteng Area itself. Incidentally, it should be mentioned that the giarmite

iutrusisc here seems to be of relatively younger ag: than that of the Yuannn-Yungen are?. According to Lu and Pai, the Upper Peuinian basaltic IaY is

again absent in this region.

"RED BßDS" OF EASThRN VUNNAN

1 will i' be out place to mention the fact that the "Red Beds sshich

oeer!ie the Gi4vtopterL-bearing Loping Coal Series in Eastern munnmn on theeast of the line- of the western limit of the Gigantopteris flora given by V. K.l'ing and A. W. (Jrabau [26, fig. 2, and prolonged further southward hitoindo-China by J. Coggin Brown f, pI. 29), cannot le compared and correlatedwith the 'Red Beds'' of Central and \Vestern Yurmntis composed of the Lufengand the Shihtnen Series as previously practiced [26, sectiOn nos. is and seIthough both may possess the common character of being salifcrous iii certain

horizons. This generalization is based upon the previous arid more recentobservations of various geologists who worked in that area which del sutci'z

indicate the 'Red Beds'' of Eastern Yuunmtn jo be the Feihsienkuan ShaH

facies of an inland-basin or a imtioral phase pertaining tu the Yehlangian inthe redefined sense of T. H. Yin [sn] which desigtates the Lower Triassic ofSouthwestern China.

RSUM OF RCNT OBSRVAT(ONS

tn) The Lufcng Series with characteristic Upper l'rmassic tetrapod

fossils in its lower part overlies a variable substratum. From the west- to theast, the following observations may be given:-

t. ': ft 2. Ueterrnnel by 'r. y, Hs.

Nus. 241 ed BcgJs o;

( i) CO11h ocries Usc Ip Uau: Cual n tr we-.rr parrfrom Elsiangyun to

b) Sharp.y unconformable on Siniau rocks a t Lofe ng or 1'eg10aueianorphosed Lalaeootc ( ) shaks at north u Yenhaingthe central part.

(e) Unconformable on Various Pakozoic rocks between Imen aridKunyang.

(d) Disconfortnably over the Upper Permian volcanic series in theeastern part around Kunming, or on Anthracolithic limestom lfl

the Hosi-Cliuchi region.

() The lithology and the fauna of the Lower Lufeng Series semindicate the sediments to be ctcnsive basia accumu'ations with marginal piedmOntdeposits, while th Upper Lufeng Series with calcarcous clays and limestonebands as well as the intermingling of marine tharks and freshwater Uioidsappear to be deposits of a brackish water ori;it in an estuirinc environa'nt.

() The Luf eng Series may be completely or partly represented atdifferent localities, while the Shihmeii Series may or may not be present.When present, the Shihmen Series always behave sympathetically with its underlying Lufeng Series in the major structural trends.

() The pre-Lufeng uncouformtty and dis;onforinity indicate an impoltantperiod of deformation falling between the Upper Permian and the Upper I'rias.

() The orogenic inöveinent that has infoded the Lufeng and theShihmen Series into a series of arcuate or elongated synclines is distinctly p051Shibtnta and pre-Plio-Pleistocene.

The 'Red l3eds'' of Central and Western Yunnan o the Lucfli.and the Shihmen types differ widely in age and facies from those of EasternYunnasi of the Feihsienkuau aspect. thaugh they are somcwhat similar LiThey arc separated from each other by a distinct barrier of older rocks.

Subordinately, it is of interest to tnerittosi the fact. which is

indirectly revealed by the study of "Red Beds', that there i a conspicuouSabsence of Upper l'ermian okauic series irom the meridirial tract of land

j; (jf' ,.'),, :

eco the 1' SL slid ib: Tn and iiiJiaus ri 's oats-s isid

-is .s'l)s'ssssie region sis Sik-tii ri cs'ilirast (o seeui c:-,1csIçrvc lsclnzoiIlal driutsn-05 CIlS scliy r. K. I bang I5, H. v) \'. . I ng nid A. \\. ;L,.

es, tld. :J. \Vlicthcs this absence is easiscd fr tu csulr'il.il noul-c:istcsi,c I

a regill viiscli scpar-atd I Wo distiiit area.s ut Silcaili,: aCtiVilul.s ir by

cuilpIetc isesnuval rcsufscit jiurn sbcjueiit esos; it-s is t pibIvin tu be cluJdstL-¡ utuni. uieta sled studie:,,

D!SCU5Sk)NS

I 11E 5115. Ilnn.U'1t1 POSi1l'N 0!' ((LE ICLNOI.5Nr C"\L LIE':. -litt the age of the Ipingtang Coal Series ihcrc see nss tr be no 9uesnin ill

e-itisidcriig it lot younger tiens Keuper sr actually None iii the píiigisngrr;ion of ihc Lufeng Ares, but difFiculties itninedirtiely arise svhest a'.iuin1ltilsr.; r

Will u-nr rclatis,n. because tise Idisglaisg auf Ysiuiuiii floras show overu 1et:IiL f t:snïsitit,nfv :s..:ceirsej Rh se'.i-Lias,i' cletsleisi.s. L'ire qscsi iii 'it 'vhvtls:these ars: livri or several nrajor Mesozoic coal'fornuise ¡rcuscsrls or 'ni''usudly advocated imis tediatci y comes forward, ru the hitter crise, the age

clesigsatiun has to be aijusted. The same question has been asked independesitiby T. Y. 1-Isu [x 2J whose works mainly concern marine Triassic fossils.

furthermore, che so.cahled Tongking Íbra uf I uuslo-Cisinri which seems iche a nucleus for comparison ut Mesozoic plants, formerly regarded as lLhacti

has nosy been considered by sonic as of None age (see p. 164). A-gain, the titlerf a paper by 'I'. Kobayashi of Japan which reads 'On the None age of theN arisva flora of the Rhacto-Liassic aspect'' ' is eloquent in itself and shouldnot be icit unmentioned.

I feet that she time has come for a general clarification of this probleissby the combined edorts of paleobotanists and paleozoölogists working either inthe invertebrate or the vertebrate fields. With a critical weighing andrcojsciI ittion of vidcnces oE tise different parties, a relatively more isaturaf basisof ciassiuicatiolu sissy lie attained iii spite of the general belief that a trueidiustuserit of conflicting facts is task next to impossibility.

'['he sriginat paper 1rsnsed in the Japanese journal ut ieoogy ant heOn5rcpInVt-2, p. l-12 n 1938 has trot beets received or ceusulted and tine iii le is cited trou p. 15-i

y' ' :,i,ji-.yr nf lud u: t (.eilr,y cxliii 5'' , .'«'- 'in ., n.-', I':'' ini. ô-l" 19,y -....i3 ut y-onu ce in 1939,

2-1 i'c/2:"Jro /eI o;r3

a1 ii DIVCISSL YA TilL "RED dSLl S kL 'il DEPOS11Yuu'ia I tKccomparative study of the "Red lieds'' la the suirouridiug regm05

1 Lowcr Lu nSzechuan, French foJa China, Fdcratd Shan StOICS. Siam aliol'as bccn on 'le he

J . oggin Brow0 4. p. 541- TlsroUSul t 115

u'ly bmouo Rthe diverse nat ore of the di ifere rt 'Red geds'' has been vigorooct. This is one point that has been vaguc!'t emphasized. in the prScflt I 110 J

- ijr the her'iShiug just the single case at the tctr.ipo'J fossils recovcreu -

that rincesBcds" at different localities, there is a diversity in geologicfrtun Lower Triassjc to Upper Crelaceous as revealed by the 1dentth1 .itcjlatc

so« h attemilinsremains. This brings out, at least, the usvudj1s5 or hiC risk o -,,of sitho-og::a long-rane coreclatmon of the "Red Lieds' on the sifl5iC C3C1

arisoli. ltstratigraphy which may be of service in short-arige regional «O-0fl13I b - 'Itbís in mind, future investigations on the "Red Beds'' should be iiiace y.s

combined analyses oC petrographic, paico1lIoiuie and stratigraplllC StUics.downwill certainly bring the present af.parcnt comnlcxitvf chaotic Cvi

h real simplicity of orderly facts.

POST-SWHMEN OROGENIC MOVEMENT, YENs1j,5\51A OR

dly mnphasizcdunportance of the post-Shihmen orogenmc rnavemsflt has been repeatC' bin the preceding sections. Although more stratigraphie evidenc hase een

arc stial srgathered lately, yet for an accurate dating of this tuovernent they. elasticitY foi agefrom being satisfactory. It is stilt in the stage of considerabc

designation that depends primarily on personal preference or taSth Cluua to beV. K. f mug believes the last orogenic process im' $out

Yeusbanjan and denies the- possibility of its being HimalayanCuriously enough, W. H. Wong, the author of the LiflLi t,

'd TertiarY periodfavors a consideration of the l'sipurtance amid existence of a R'l -

of intense mountain building in South China [o j.rtiar\' disturbanceElsewhere 2 j, I have given evidences of the !rnmd- jC

, ofhiclm is called the Ilcugyanelan nIovclucilt in the rcdelincu $

i . called forth aYOung, M.. N'. Bien and Y. Y. Lre 134 J n iliunan. I hisI ( there ischorus of disapproval, because it his bceu pmuvcd locally t tts and therefoichorizontal movement after the deposition of Early Tertiary scdiUhCfl

it cannot be of orogcnic nature, which is a mn mtl r of defmui tiOi'ad the «ritical1. 1 lie liberty o oint: 111g n'IO u Lie Ci ...c. is-. ,;.i In beu t'-í

paper.reads; is sd t: ts c,ju. 5hScg-apby sjsei,i u ii br

l,uI,-/;tj 0] !/i. ,cíc of (i/I'll

flic l)u5t-SliIlunen deformation is indeed (eitui: satu I jur.fc

to ecustder it as a mid Tertiary event or the IJe;'.gytn,s.iu 1suveucn \s thundisturbed materials after the pust hi .nn disturaticc arc ut Pl iPiei5Lo2cn

age, it is just as difficult for the advocates of the Vcushauian inove;s-int tt'proe it as to disprove the existence of the I ienyang.t 1 orogenic phase, t

Chinese manifestation of the Himalayan, in the hastrophic history ol Yurtuan,

OF rice ecija.

Thc iiifolding of the "Red Beds" of Central Yunnais iuto a cric

ar.uate or southerly converging elongated synclines accompanied h tbristin;.caused by the post-Siiihtnen deformation appear to fit \vell with iii: slructur.

echerne known as the "Pakng epsilon system oL shear form" proposed by J. S. Leu. p.308-31 t), though I may be accused of being eclectic. With the i nplicatmo

mhmi tiic Pakang system has been distorted by the powerful eta system onwest and that they impinge along the great Red Rivai fault, the slrimcturcs ilk

the northern Nt of the lake region Ust mentioned and those of the Luíen

Area seem to lie in the zone of compression in the rear part of the Yunnanarc, a small portion of the naia system. while the J.Jiju tims-cid :UL by Live

aysicms of faults with injections of granite 1201 SCCflI to be the extreme frontalpart of the apex that ha ticen sitbected to tension.

'I'he arms of the Triassic sea known as the ''Guite de Yummnami.I'' and

the "Golfe d'Ami Tchou'' which converge to the south as postulated by J.Froniaget f to] seem to be the forerunner of the Yonnais arc in the querionof both linac and structure, if we grant that marine troughs or geosynclines areformed by lateral compression. This means that the active crustai stress iii thit

LOr1 followed a quite definite movement cer since the f'riassic time o even

cartier. And, moreover, the course of this mavenut svas not in the leasefortuitous, and reached jis acme in the pu -Shihn.n time represented by the1--lcngyanïais orogenic movement.

CONCLUSION

Tise ' 'Red Beds'' of Central and Weitern Yummiman a re ds ,dcd into theLuterig Series of Upper Triassic age and the Shihmmaen Series of quctionableJ ura-Cretaceous age. They are separated from each other by a disconformity,amid diflercnt from the ''Red Beds o Eastern Yumanam.

'Ph post-Shihtnen orogenme ni vemeat n'sy be Ye,mshw.m n ti

but tht latter is thc mrcfcrred urm.

2 4 ' J'? i'd'' t;i

gIRENClis

fsers, \I \ l).li. e.Iogv of the' Via'ev atm, rnion. Ril. Ct'7/ Ç5' C1, t.'.E')I. NX. no. I, i.

- . j 91(. Plhninar' cil'ers'atios' on t)e Cenosoic Genlory f Vinn. li'.!'-20l.

1940. Discovery of Tria.ic Serischian e'nd Priniti.e 1tteremalian

nfnn', \t'nn:rn. !.i.,. tos. 3 4, p. 22-218.

n n, J. Cogin, 1938. Coutrihuti,io t' the Geology of the Pro.'itCe of Y y

\\ c-stotn (¡mu (10) The distribution, açe tend re!ationshipc f t!e re li J-. '- -.

(;l, Sure'. Indio, vol. 73, pt. 4, p. 314-570.

(:h?n, 1933. On thé ubdjvjsjony of tir Red Beds of Soth-Eastern Chico.G'.o. r11. v. Vi11, nos. 3 & 4, p. 3fl l-32) -

, (mn. T. O., 1927 (. 'ii.Cre'insr, W. I (3, Ob.:ervatiotcs on Geology end Morphology of Vunnan. G:ti. .s re'.

Kwt;:rfun and Ka'an''i, See'. Py4,, no. 10.tcp 'I oit, AleN. I,,, 1926. TIte (7ee'io'': Soyr/i liria. Published he' OUoet n.) l9ods

Fci'')rirgh.g, Fu,.j. k. '.. and Kuo, W. K., 19. ...t, E'n:eget, J., 1929. Not préliminaire sur Is Stratigraphie de Formations

eir l'âge des M')u'enents mtjcirc en lcd chine Bull. .Çrr. GoI. ¡/,f(hj?t, vol.

rviij, fase. 5.

II. hice'. . and jCiCt5, I".., 13 1, Syecha-Ti!cet-E'.j.'yd;tOSN der Steti Yatsen

I aivsr'itt, Canton. Zschr. Ges. f. Erdk., no. 7-S.!2. Hen. T. Y., 1439. tV13. 1940. 467-474.

¡4.. Han, T. Y. nd Pien, C. S., 1940,

Ic. Hunf, T. K., 1932. The Permian Formations of 4outhern China. Mc,n: G-o!. Sure'.

Chie's, ser. A. no. hO.

16. bang, Y. s., 1940. Ge& gy of the iron deposits of Ornen, Yunnan. Bull. Gol. Suri'.

no. 33, p.'65-36 (Chinese), p. 25-26 (Eceghish summ.).

i, Krejci.Gral, K., 1934. Geologie des gebietes s',s'ischecc Yünnanfu und deen \'tngte l':igNord ''ecnnan, Chin;'). Gn1, R'ndschazc. 'cxv }Sd., 1-Seit S, s. 305-312.

5 1.t'e L S..1939. The Geologe' of China. Published by Tiomas Murbv & Co., 1.mcdon.

¡9, In, C. l-1. and PaL C. C., 1939, Jirn.If 3)3-346.

20. Tng. U, M.. Clcerr,. K a'itj H, 'I'., l36-3'. Geojoy of Cie Kachiu tiri-fild, Yctntc.iec

.\ i.rljaIhtsi ' tketCc L Bu!!, C: i'.'. Si. C/time, s'1, XVI 'E'he V. K. Ting Maio.i ia!

p. '121-437,

4:yn_gc-(ituT1, ".'- .: ir 01 kI i-'.OIC L' 'i. o

iJ I'. Soc. ¡:, ii ., ,, , 4 p

° 13111. C'ilngy of Sivaiigt.,rlg cal fielt, Si, alit iti.tl:! 1);:/i. C!.Sor,. ('/,iml, 'ti, p. 59-63 (Ctinese, p. 2 EiigIih ininui. 1.

.S;tl,,,i, P., 1936. \Vegene; 's ttteoi ' nf ('oi,fi:ental dr,) in tt, light 'f 'al w'l,o:i,,i.Jience. /aji.. lui. So'. Soc., vI. IS, in. 5, ,. 3l-3:)2,

Sn, rin, E., 1)33. Ohscrv at h ns gbolo'.i p IN Cuti C Yut,nanfoi et Vita n Vi np 4' ii

Vunnait ) Bull. Soc, (7,1,?, Fr,,,tce, 4e 4i ., t, 3 '. 441-4 3.

Iitt4, V, Is., 1929. 'Fhe Origetile M,'. Cn,ets lit China. 11J1, Gee!. Soc. Chin, , el.VII), no, 2, .p. I 51-170.

anti Graben, A. W. 1934. Tic Peru,iaii ' China aid its ilearin,' in Pet oisflla..ificatioa. Sept. XT'I Tntrn. C'al. C',: . \\'a7,ïn.r4,,r,, 1933.

27. Tevap, '1'. C., 1*4', J 11l i'ViJtfl, 'I 117.133,

2). 'S' tii, I . C,, 4 U.0 G5iiio7v in tile enrir,n',ieiii it Ilttitiiiiiig. lOt), .\,inlverssrs' lape (JI

the \iti,,ial T.';iio:ii' of Pekinp.29. Vt'rg, \'. I.., 19 i'.. li'o ore tIc,.ilïts , f Kut,va,t.', t'),.Itait, VIRIlI, CI,,,s'I,i tui

l.iiigtvuu disrirts, \'uiiitan, il::ll, 'C:.'/, Sort'. C/isa, ii) .43, p 47.47

2 J 3i) (English st,,tiuii.

30. Wisttg, W, H., 1927, Ct,tstal movements and igneous actisities in Eacte, t: China slii:c2,ieene,'i,' die. Bull. Genl. Soc. China, t'ol. VI, ito. I, p. 9-36.

2f. 'ile, '1'. H., 1532. Vcl,iasini,, lippes Perrulan cur l.o,si Tria-sic? ¡lid, sol. XVII, nos.,3 & 4, p. 249.:) 42.

:i 7. Young, 17. C., 1937. New Triassic and Cretace,,u Reptiles iii China. ¡l'id. ml. X\'Ii,p. 109-120.

33. --- -, 1937. On die Triassic Dicynodonts from Shansi. ¡bid. 3 & 4, p. 393.112.3-4, , Ben, M. N. and Lee, Y. V., 1934. ''Red Beds'' of linean. Ibid., v,,I. XVIII,

no'. .3 & 4, p 259-33i1.

35. , 1439, fjt,f9 94.94,

3o. --- -, 1339. Pseliminaty Note on the I.nfeng Sauris,'];iu:t en,ains. 4'tth Anniveratypapers of the National University of Peking.

2 . , 1910. Pseliminiry Notes on the Mes'z,ic Maternais ut 1_tifeng, \'uttttau. Diii!.()eoi. So,'. Chiot, vol. XX, no. 1, 93.111.

- , 1941). Preliutiinary Note on the !.ufeng \ettel,rat fossils. Iuid to:. 3 5 4,p. 235-239.

3'),, 1941. On two new fossil f dico front Soutbwestru Cltina. ¡l'id., 2Xi,

t". 1, p. Sl 91,.4 (t, -, 1941. c;yposaurt,s sinensis (sp. nov.). A new I'rosnuuropoda froni tl,e U 'ter

Triassic beds at I.uifeng, Vunnan. Ibid. Vol. XXI, Nos. 2-1, p. 205-252.li - - , 1''4 I. ïunneiio:uruc liulilgi (gen. et :. to,.), ,1, Aew I'rosa,,ro1,c,,ia lion, tite

lvd ¡ ed, at ¡.ufeng, \'unnau,. MS.t.:. -, ¡941 - Aconii'iete o'.ieol.' il Lfco,o.iumu.o .S:cn,-j Voting (get,. ni op. lo,.).

1','!,;o,,!../j.i Sr::,.:, .,v ..,ic, ii. ., 'ii.. .rJc:' 7'I, t,id 35 Sxt'fi.'uiiN 3, 4, olei

rz:--Red Be" of Ywtrn

'4

LUF ENG J-'.t&

w.tc c'9oaa

r

', :1

Hogc,,cheo

1pchan9

[1adm os5 ferv s&

Fig. I.- A 9erIereI view of the eastern part of the Lufen9 Are n the fore-ground are hIs of pre-Carnbrion rocks foflod by much dissec hiH ofdu% I purp '.sh nd dark red beds of the Upper Trissic Lower Luf Series upto the Itne occupied by Huanchiatien. The siopes beneath the prominent es-carpment ore composed of 9reenish-ye low handed, variegated end wine-red bedsof the Upper Lufen9 Series, while the escarpment itself Is formcc by tie sand-stones of the 3hihmen Series. The much 9u1 t ied hi I Is around Huagtupo areformed by the sate Tertiary sandy beds.

...................

F. 2.- Lookjn9 northward from the Shawan fossitjferous site towards theTachung site. Hill on the left composed mainly cl pre-Cwnbrian phyll tes.The contact between the Lufen9 Series arid the pro-Cambrian rocks lies at themuch 9u1 lied oreo. Thê different beds of the Lufeng Series on the rght Showa progressive decrease in dip towords the east. (From photos YlbI 4-6,Dec.2,S939)

w ochentiio

¡V:

H i3tuf o

Ighway-" ---Fig. 3.- Looking northword from thelow pass south 'of (aochientsao. Show-ing the pro3resaive overfolding ofthe greenish-yellow banded and varie-gated beds of the Upper Lufeng Seriestowards the north and aso the graduatdecrease in intensity o dip towardsthe east. (From photo '(I b I 9, Dec.17, 1939).

w

<tV'.z:V .,.J-Fig. 4.- Lool<ing northward from pass south of Yaochan. Showing the gate-likegap which the main road to Lufeng penetrates in the Shihmen sandstones at Shih-menshao and the gentle slopes formed by the variegated and wine-red beds ofthe Upper Lufeng Series.

l<aochient600

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Dec. 2i. iqiq

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Plate I

r

n,........

Bjen:"Rcd Bcdc" of Yunnan

GEOLOGIC MAP 0F THE ANNING BASI,"'UI4NA(1940)

TepoGptir FD JPO f5OOOO IIAF'5 OF TOC Yurs t..po 5uc JLNB.4O

6

z

-C

EX PL ANA1]ON

H0

Otbt Itwab . Jip

Platc lU

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LI.WE 146 5Es M.4.

"o.Stnr. _

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F'ooIif-. set.

BJen:'Red Beds'' (f Yunnan

i_,o,:.u 15 LUkO

Ç.

let ce. cct,tects

Noo,to n4 ?!Ct$t{it.recbon of

GEOLOGiC MAP OF ThE LUFENG AREA ,YUNNAP4

OE-oGY M.N.Bs(1939)IPtNGLAI'IG REG)ON BASE.D UPON fllE WORP( B'1'

H. S.Wo ,T. C. Ciáu, CH. Lu,'i' HuANO ANP C. C.P.i&

I 2 3 4 5 LOMETER5

O,,rtht f,utotot.l4p

letr fIt

riI2 u,tI

Fss,IirI45trK o4ogo-tose4 4p

_________ p&r- tipnri i. inn r r is& tMtn Sugv

EXPLAATL ON

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r..

Q'doefr,san4 ¡ ckys

.?JIC:. S*IIflMEISERIE5 C.u-bedIeIs...Çi(.,,d

LUFENG SERIES 5,,dst,is, sb*'.s £

&.sd.S.ccias

IP1NGLANG COA.L SERIES S.,,I,tones,shm/e,&c/aedms

FWte4,qua,t.z,te.i,C(ySt.JJ.e /.t,A'.oS,"'c- 'd eto.

H

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Plate II