Decis沙 on 嚓 Lochkovian A-W }j 一.rragian rDounciary Stratotype (Low er D evon ia n )

妙 Ivo Chlup k and W illiam A . O liver, Jr.

T he Global Stratotype Section and Point (G SSP) for the represent a p r o g r e s sio n from low to high energy environ- Lochkovian-Pragian Stage (m iddle Low er D evonian) has now m e n t s. C e rna ro kle h a s the best m egafauna w hile C ik5nka been agreed upon. The boundary is defined at the first Q uarry h a s t h e m o s t a b u n d a n t c o n o d o n t fauna. Velkg occurrence of the zone conodont Eognathodus sulcatus C h u c h le is inte rm e d ia te a nd w as s e le c te d as stratotype sulcatus at the base of bed 12 in the V elkfi C huchle Q uarry, b e c a u se of the good interm ixture of conodonts and m ega- 下丽万而rthwest part of Prague, Czechoslovakia. fo s s ils. R anges key species a t th e t hre e lo ca litie s a r e v e ry In tro du ctio n of sim ilar; a L each locality the 翌竺丝些 boundary is a sh o rt The Low er D evonian stages, from oldest to youngest, are d ist a n c e b e lo w t h e p reviously accepted m egafossil Lochkovian, P ragian, and Em sian. The base of the Loch- bounda四． ChlupA6 and others (1985) published e x t e n s iv e ko via n co inc ide s w ith the ba se o f th e L o w e r D evo n ian S eries range charts and lists of fossils from these a n d o t h e r and of the D evonian System and has been form ally defined boundary sections, together w ith discussions of the as the Silurian-D evonian boundary (M artinsson, ed., 1977). stratigraphic significance and usefulness of the m ajor groups The boundary betw een the Lochkovian and the Pragian is the of fossils of the Lochkovian-Pragian interval. subject of this paper. That betw een the Pragian and Em sian is undefined and is the subject of ongoing discussions w ithin T he boundary is closely related to an event-stratigraphy level of probable global im portance, nam ely the "Loch- the International Subcom m ission on D evonian Stratigraphy kovian-P ragian Boundary E vent," w hich, how ever, lies close (SD S), a unit of the International C om m ission on Stratig- above the Pragian base. T his event-boundary (m ost likely a raphy (ICS) of IU GS. The nam es of the Lower D evonian e u s ta t ic fall in sea level) m ay be useful i n identifying the Stages w ere adopted by SD S in 1983, recom m ended to IC S in b ro a d e r boundary interval on w o rld w id e scale (co m pare 1984, and ratified by IU G S in 1985 (Bassett, 1985). ，a In． Ia Johnson, M apper and the interval before Cycle In． R egional Setting Sandberg 1985, and applications the stratotype area, in C hlupA6 and K ukal 1986, 1988). Paleom agnetic studies a r e T he boundary beds have been studied in detail at several in progress by D r. M . K rs in Prague. P relim inary results localities in the B arrandian area, southw est of Prague su gg est t hat tne ve tKa 七h uc hle sec tio n ha s b ee n (F ig. 1). Three localities w ere described in detail by both rem agnetized. T he color alteration index of VelkA C buchle W eddigQ.0 987) and ChlupA6, Lukeg and W eddige (1988). The conodonts is 3 (Sch6nlaub, w ritten com m unication, 1989). three, C ernA rokle, V elkA C huchle and C ikfinka Q uarry,

乙少户 Prior to the nam ing of the Pragian Stage in 1958 and its －‘甲－厂一厂N ～es 尸‘es 一一－厂－ 七产只代 了－又 acceptance by SD S in 1983, the "Siegenian Stage" w as used 芙 by m any w orkers for the m iddle stage o f the Low er 一 P R A H A D evonian. This w as based on benthic, near-shore fossils, p rincipally brachiopods, and w as sufficiently useful up to about 1950 w hen pelagic fossils such as conodonts began to V elk6 C hu chle predom inate in long-range correlations. W ith continuing I 伙a R B E R O U N 降 refinem ent of intercontinental correlations, it becam e clear 洲 马、 that the I'Siegenian Stage" could not be satisfactorily 冲创 defined in its type area (W est G erm any) and the shift to ｝1 P ragian resulted. R ecent studies in northern Spain, B rittany and W est G erm any show that the base of the Pragian is nearly correl- ative w ith the base of the "Siegenian" in the sense of C arls 。一}1_1 I (1987). O ne option w ould have been to select a G SSP for the R O K YC A N Y ｝！ I 称舒 "Siegenian" in a pelagic facies (e.g., C zechoslovakia), but the SD S decision to use the term "Pragian" reflects the feeling that the term "Siegenian" is too closely regarded in 邓 term s of a R henish, near-shore clastic, benthic facies, 1 0 2 0 k m ‘ 一一一」 w hereas "P ragian" signifies a diverse fossil assem blage that includes w idespread pelagic fossils. 1田11 2F刀 3区次｝注一墓 I I二口 6压 团 7国 。口 B oundary Stratotype (G SSP ) Figure 1 : Geographic and geologic setting of the stratotype section in the Barrandian area of cen tral T he position of the Lochkovian-Pragian boundary and the B oh em ia . 1 一 Pr o ter o zo ic , 2 - Cam b ria n , 3- O rd ov ic i an , G SSP for it w ere accepted by the International Subcom m is- 4- Silurian and Devonian, 5- m etamorphic Proterozoic sion on D evonian Stratigrap hy in A ugust-O ctober 1988, and and lower Paleozoic, 6- granitoids, 7- continental approved by the International C om m ission on Stratigraphy Upper Carboniferous, 8- 〔孕per Cretaceous and and ratified by the Executive C om m ittee of IU G S during Te rti a ry s ed im en ta ry r ock s . Januarv-F ebruary 1989. T he stratotype is to be m arked by

E PISO D ES, Vol. 12, N o. 2, June 1989 1 0 9 a plaque w ith explanation, and a perm anent m etal line is to planes are knobby; the characteristic nodular structure is be inserted in the rock face at the boundary. M arking and developed in m icrites and biom icrites with Chondrites m aintenance w ill be done by the G eological Survey of burrow s that start 2 to 3 m above the stage boundary. C zechoslovakia, in collaboration w ith the C enter for Natural R eserves, also in Prague. B oundary L evel (base of Pragian) T he G SS P of the sulcatus boundary is in southw estern T he stage boundary w as chosen by SD S in 1988 to coincide Prague, in the secti而不r e_IkA C huchle (Fig. 1). This is an w ith the low er boundary of the Eognathodus sulcatus cono- old quarry 。。 ihp rnqri from Praha-VeIkA C huchle to dont Zone defined by the first occurrence of 互.一s ulca生us S liv e n e c o n V dolich Street V fdoli), 8 km southw est of the sulca生矍 P hilip, 1965. In som e discussions this has been city center. T he quarry is on the nature reserve called referred to as the sulcatus boundary. The E . sulcatus Z one "H om olka," in the district of Prague 5; the distance from a w as fi rst defined by Fahraeus, 1971, and has since been city bus term inus is about 400 m (Figs. 2 and 3). In the accepted as part of the standard conodont zonal sequence (K Iapper and Johnson, 1982). T he nam e taxon and zone are VeIk9 C huchle section, the stage boundary is defined as the base of B ed 12, at the first occurrence of E. suicatus now recognized in C zechoslovakia, G erm any, A ustria, su lc a tu s. C hina, A ustralia, U .S.A . (N evada, A laska) and C anada (see W eddige, 1987, p. 484-5, for details). A lthough nearly w orld-w ide in distribution, it has not yet been recorded or 一‘} M C I6 ／“ recognized in the Soviet U nion or eastern N o rth A m erica. ／下，‘，Ch些}I T hese are m ajor geograp hic gaps, but it seem s likely that 匕二，’ the form er, at least, w ill be filled. M axim um provincialism ＼ and inappropriate lithofacies in eastern N orth A m erica 、 爪 个 小个 小‘｛ m ake it less likely that the zone w ill be recognized in this 。 ＿＿． ）， area, but other criteria perm it approxim ate correlations. S liv e n e c 少夕12几一，气“， E . sulcatus sulcatus is thought to be part of a lineage that /P'/O/OVI 孙 strofotype } 勺 ‘与今 今 proceeds from O zarkodina pandora (early and late form s) to HomoIlka ， E. sulcatus (early and late form s). A series of m orphotypes VelkaI C huchle described in each species has biostratigraphic usefulness (M urphy, M atti and W alliser, 1981). The general sequence in the Pragian type region is illustrated by W eddige (1987, figs. 孜V软_4, Vy D}701-1. rO O 2-6). T he defining m orphologic character of the earliest ＿万，少全 sulcatus is rem arkably clear (W eddige, 1987, p. 481). 乙‘ ＿ 呻尹 G raptolite zonation. The boundary level lies above the graptolite Z one w ith M onograptus hercynicus, w hich is 行＂ traditionally included in the upper Lochkovian. N early L o c h k o v 仇 ' 9t z}' w orldw ide in distribution, it is know n from C zechoslovakia, Thuringia, the C arnic A lps, Y ugoslavia, B ulgaria, Sardina, 0 1k m ，匹二刁2巨二困：尹 ‘了 5厂 ． I N W A frica, the northern U ral m ountains, F ergana, C entral A sia, M alaya, T hailand, South C hina, A laska, and w estern Figure 2: Map of immediate vicinity of Velk5 N orth A m erica (Jaeger, 1979; K oren, 1979). Chuchle and the stratotype section . 1一urbanized D acryoconarid (tentaculite) zonation. T he boundary is areas, 2- forests , 3- highways, 4- railway, 5- above the Paranow akia interm edia Zone, w hich is tradi- b r o o .k s . tionally included in the upper Lochkovian and is also w ide- spread (Europe, northw est A frica, A sia, and A ustralia). T he base of the subsequent Z one w ith N ow akia sororcula (possi- The outcrops have been studied since B arrande's tim e (early bly 二N. kabylica， see Alberti, 1988T- lie,币而而面ow the 19th century), and the structure w as clarified in the second half of the 19th century. B iostratigraphic studies of the 劫 ． Lochkovian and Pragian were carried out by ChlupA6 in the ． 1950s, and detailed investigation of the boundary interval by 5 ［iv e n e c C hlupA6, Luke}, Paris and Sch6nlaub (1985) and W eddige (1987). T he outcrop w as visited by the D evonian Subcom - m ission in 1986 (described in Chlupg6, Hladil, and Lukeg, 1986). The outcrop exposes a synclinal structure form ed by Loch- kovian strata (lim bs) and Pragian strata (core). The Lochkovian-Pragian boundary beds are exposed in both w estern and eastern lim bs of the syncline. The section on the w estern side, w here the beds form several sim ple folds, is the stratotype (F igs. 4, 5). In the eastern lim b of the syncline the beds are vertical. T he upper Lochkovian consists of gray, fine-grained, blo- detrital, bitum inous platy lim estones w ith uncom m on cherts 皱 叮 and subordinate very thin intercalations of calcareous m ud- 户 ． 赛 sto n e be ds th a t are m illim etre s to a few c en tim etre s th ic k. 侧 T he Lochkovian-Pragian boundary, based on the first occur- 引 巍 以、 权 rence of Eognathodus sulcatus, lies w ithin this sequence, w hich show s no m arked lithologic change. Except for its low est part, the Pragian sequence is repre- 0 5 0 0 m sented by the D vorce-Prokop L im estone. This is light gray, biom icritic to finely biodetrital in the low est part and passes upw ard into darker gray m icritic lim estones. Bedding Figure 3: D etailed map of stratotype location.

110 EPISO D ES, Vol. 12, No. 2, June 1989 汀 竿 F o ssils 淡 终 The occurrences of conodonts, chitinozoans and other index 瀑 黔骥 邵 爹妾 fossils are sum m arized in Figure 6 and detailed in F igure 7. 鑫 一奢 攀 徽 The upperm ost Lochkovian contains m ostly fragm ental m a cro fossils ide ntica l w ith those fro m other nearby lo c a litie s : t rilo b it e s (L e Dido, ro e t u s Ie idus lepidus, R a n u n c U lO D r o e t u s he te roc ly tus, L e o n a s loc h k ov en sis, S D in isc u te llu m Iasi, a n d s m a ll chonetid, strophom enid ind ex A reo stro }h ia interjecta, a n d others), atrypid and rhynchnonel-lid brachiopods; thin-shelled 了 r1 l_ bivalves ( Neklania, Hercynella, Panenka), g astropods, nautiloids, phyllocarids, etc. T he characteristic upper L oc h ko vian m a c ro fo ssils co ntinu e u p in to b ed N o. 12. tha t is above the first occurrence of Eognathodus sulcatus.

A A : re d e f in e d b o u n d a ry 几t ra d it io n a l b o u n d a ry la te up per Lo ch kovio n ！一ow er Pra gia n 。 9 Fi g ure 4 : Vi e w o f th e wall of the old quarry. A--A O， M on og rop tus h ercy n ic us P m a r k s the b o un da r y in te rv al s ho wn i n F ig ur e 5 . t M on .kays eri 冲 e boundary, w hile the low est occurrence of typical specim ens n 冲 Poranowok‘口intermedia 州一— － O of the w orldw ide Pragian index N ow akia acuaria s.s. is O ab o ve the bo u nd a rv : N . c f. a cu a ria o cc u rs b e lo w th e N ow a k ic s o ro rc u to C 一 I一 一 二 o ou na ary tsee L;niup a c, L U KeS, F aris a na z!icn o nlau l), IV 60). 巾 N. acuaria is known from Europe (Bohem ia, Thuringia, ！ 5 Franconia, M oravia, H arz M ts., R hineland, Spain, Sardinia, N OW lacuorio 一一》 C arnic A lps, A m orican M assif), A sia (U rals, C entral A sia, Siberia, Burm a, T ibet, C hina), northw est A frica (M orocco, O z a r k o d in a r e m s c h e id e n s is C A lgeria), N orth A m erica (A laska, C anadian A rctic) and O A ustralia (see sum m aries of occurrences in A lberti, 1979, 口 O d 1987, LUtke 1979, 1985). O L a te ric r io d u s s p.n .A ， C h itino zo an zo na tio n. T h is is th e t m ost pro m ising m ethod s for the correlation of terrigenous elastic an d no n- m a rine L o te ric r . s te in o c h e n s is sequences. T he boundary falls just below the low est o c c u r - P e d a v is p e s a v is rence o f the Pragian index A ngochitina com osa c lo s e to th e f ir st o c c u r r e n c e o f G o t la n d o c h itin a h ili oti, a n d c lo se t o 0 2 p a n d o r o the last occurrence of Eisenackitina bohem ica (Paris, 1981 门 and in C hluDA6 et al.. 19-8-5犷一一一一一一一一— ︸ s te in h o r n e n s is O h It is inevitable that som e o f the ranges show n for taxa in the 一 ～ A 一 n t VelkA C huchle section w ill prove to be incom plete w hen A n go ch itino c o 印 0 S Q 刀︸ 0 studied on a w orldw ide basis, but the correlation potential 2 M a rgachitino c o te n o r 旧 c o t e n o r ia 0 of the boundary level is w orldw ide and can be approxim ated 0 二 by m eans of several different groups of fossils w ith inter- M. catenariai tenuipes 一－－一 ） 5 c o n t in e n t a l d is tr ib u t io n . G o t ta n d o c h itin o ro m o s u s 1 Gott. philippoti L o c h k ov e tto m is e ro ｝ 一朴一 R eed ops tim es prog e ns is 碑 r R e ed. g r. s te rn be rg i 一 Spiniscut. um bettiferum O b S pin iScu te ltu m p to s i 冲－ e s O d o n to c h ile

Leo no sp is loc h kove ns is

P ro g o p ro e tu s . G e ra s to s

Lepidoproe tus tepid us tep id 不latyscutettum t P o ro s c u te tiu m D e c o ro s c u te ttu m ＋M e ta s c u te ltu m

Figure 6 : Ranges of selected index fossils as Figure 5: Boundary interval at stratotype curren tly known in the Lochkovian-Pra好an boundary section. The top of the white bar marks the i n t e r v a l i n t h e B a r r a n d i a n a r e a . 叨〕e i n t e r v a l s h o w n b o un da r y a t th e b a se o f be d 1 2 . Th e b ar is is app ro xim a te l y 5 m ab o ve an d b el o w th e b o un da r y . a pp r ox im a te l y 0 . 7 m lon g . R an ge s a re fro m s o u r c e s c i t e d i n th e t e x t .

EP ISO D ES, Vol. 12, No. 2, June 1989 111 s equ en c e g r e y Prokop Lim estone and the species c o n tin u es c o to u r becom es abundant about 2 m higher. 一 乌葺te n to c u tite s co n o d o nts c h itin oz . m o cro fo s The G SSP, the 塑丝蛀些 boundary at 妈 I 。 飞 I I 一 the base of bed 12 (F igs. 5, 7), is 4 ﹄ 0.1 m b elow th e trad itio na l bo un d- 口0 幻 D。 价 ｜ ～ ary, based on m egafossils, at the 妮 n一o 价 ｜ 胡 uN u base of the D vorce-Prokop Lim e- ‘ 口 阳 5 40 0O D ‘． 一 二 S一 ston e. B e d 1 2 ha s "L oc hk ov ian " 鬓 0es ﹄ O 炸 岔 。 es D D u 1 价es n 阳 口 一 38 一 es u 5 lithology and m egafauna, indicating 。es 0 一 u 切 es D 山 陌 ‘ 。 that th e a d ve nt o f E . sulca tus w a s 一 护 0 36 涅es 山 卜 卜 。． 卜 陈 二 。 l 口 u ‘ not related to local facies change. ‘ 肠 ，es 一 0 口 Oes ﹄ 山 0 N 0 和 P 轰 Nes 一 5 任 Sum m ary u es ‘ 瑟 ‘ 山 － J u n T 和 几 1 T h e E . sulc atus Z o n e is w o rld w id e in 0 0 o o es 一 召 召 0 se E 习 o ＋ 口一 q ． ‘ u 口 。 exten t and the n a m e co no do n t ha s 331- 一． n 1 D 多 ︸ 1 口 ﹄ 一︸ U－ ． d greater potential for recognition u 30 5 上 Q O 二全二了 O 的 · o ：卜 的～ u E 0 and correlation than any know n V o O 份 ‘ 29 一 o c 口 口 ﹄ D U 0 fossil that occurs anyw here near the u d 洛 D 。 O P U U a P～ 份 价 。 traditional Lochkovian-Pragian ﹄ 山 价 u 一 卜工 l 勺 2 8 一 l o n 1 D 一 d 江 丈 D 戍 C一 二1 U 上 0 ‘ V 中 。 boundary. The position of the sul- C set 。 o U 0 工 0‘ D S ＋ 卜 0 ﹄ l z 。 E一 O 0 1 cat些．boundary is 0.1 m below the 口 。27 - 典蒸去 o 5 o E 工 0 D 0 亡 u︸ O u 0 侧 n a 妇 C U 0 多 o 任 ﹄ 的 二 0 0 o traditional (m egafossil) boundary in 习 O D P 0 O 1 0 ze 1 l 工 O the type section (see Fig. 7). 1 2 5 一 切 q 。 Ol 归 仁 ︶ o 0 花 一 ． D n d D 勺 u ． u n 0 P n 23 一 l ‘ l U P 。 ． The proposed stratotype is in a P 工 D D 山 山 a l D o ： ． 口 es o C u ． 丁 n eritic fa cies o f interm e d ia te 含22－ O 二 ︸ ． U 汉 X 工 妇 一 。 O ． － ﹄ D o 和 U ． ﹂ 止20一 0 多 0 D﹄ O 1 ． ， energy level and contains a highly － 一 u 艺 涅 － 口 P P 0 ． 2 Z 的 X 口 1 l ‘ 0 j ‘ O 。 一 es d iv erse fa un a o f trad itio na l a nd P a es 一 D 。 D o U O E D ＞ es O N 山 u u U fine w " ind ex fossils. B eca use o f this ‘ ﹄ ‘ ． 的 二 O ：：二 口 0 胜 O a ． ﹄ 必 ‘ 田 a 旧 们 C 一 江 十 es P l 一 ﹄ diversity, the Pragian Stage has 八 u 山 ～ 刁 二 ｜ － se ． 0一 ． 山 to ‘ becom e the preferred standard in 杏 占 ﹄ ： 1 十 1 犯 。 一 ．人 ． － a 京 － 下 人﹂ ！法 -1 － 卜 1 m a n y w orld regions. Selection of P 的 ｜ 们－ ｜ ． 1 亏 o 1 ． ． 1 the G SSP perm its greater precision 。 o ‘ ． ． ． es 5～ 10 馨蒙 童 0 l 沐 自． 1 价 ‘ u 。 1 ‘1 l 0 in recognition of Pragian strata in 9 一 0 se ︸ u 白 ‘ ﹂ ‘ we ￡ we 1 to 0 D l a 哎 es es． ﹄ other parts of the w orld. T he G SSP ． l ． d es 口 工 人l es 0 es ． ． t 0 is on the edge of Prague, C zechoslo- ＞ 76二 es 琴 ． 月 仁 es o 自 曲 vakia, in a nature reserve w here O 幽 ‘ 幂 es N ． we es 涅 es es 右 c access is easy and preservation is es ． e 人 D es ． ． 工 上 es ． 二 ． ＞ a s su r e d . 0 es ． ． 0 es ． 自． ． 涅 厂 es ． 二 1 M A cknow ledgem ents 0 l ‘ ｜ ， 了 0 ｜ ， es 0 1 l es ︶ T h e a u tho rs are ind eb te d to othe r es es es ｜ ． es es ｜ ． 一 es ． es m e m b e rs o f the D e von ian S ub - l 土 一一 se es ． 丫 com m ission and to m any colleagues ﹀ ｛ we for discussions and help during the ｜ L tim e that SD S has been w orking on se qu en ce the L ochkovian-Pragian boundary. co n tin u e s 1口 ：雷 3国 、曰 Thanks are due J.T. D utro, Jr., A .G . H arris, and M .A . M urp勺 for review - ing an earlier draft of this paper. F i gur e 7 : C o l um n a r s e c tion o f b o und ar y in ter va l a t Ve lkA C h u c h l e Qua r ry s tra t o typ e se c tio n ;厂 l i th ol og y and ranges of key fossils a r e s h o w n . After Ch lup}6, Luke}, Paris and Sch(5nlaub (19 8 5) an d We dd i ge (1 98 7 ) w i th a dd i tio n o f ne-w d it-,i (198 8 ) 。 1 一 f i n e b io de t ri ta l to bi om ic ri ti c l im es ton e s , 2- la mi n a te d D r. 1vo C blupA6 is a senior m ic ri t es , 3 - n od u la r m i c ri te s , 4一 sha l e geologist w ith the C zechoslovakian i n t e r c a l a t i o n s . G eological Survey, (M alostransk6 nhm }stf 19, 118-21 Praha 1). H e w orks on Paleozoic (m ainly D acryoconarid tentaculites are represented by all im portant D evonian) stratigraphy, and the zonal taxa of the upper Lochkovian一ow er Pragian, and the paleontology of arthropods and sam e is true of conodonts (Figs. 6, 7). C hitinozoans are less goniatites. H e is C hairm an of the com m on 0 to 4 specim ens per gram of rock) but are also C zechoslovak Stratigraphic Com - represented by index taxa. m ission, V ice-C hairm an of the In te rn a tio nal S ub co m m issio n on T ypical Pragian m acrofossils, e. g trilobites (R eedops D evonian Stratigraphy, and a m em - prospicens, R eedops gr. sternbergi, O d o n t o c h ile h a u s m a n n i b er o f the In tern a tion al S ub co m - and allied species, C rotalocephalus lo b f r n s ， Platyscutel- m ission on Stratigraphic Classifi- lum form osum form osum ) and the brachiopod D alejodiscus c a t io n a n d s e v e r a l o t h e r in t e r- subcom itans are found in the low est 5 rn of the D vorce- national stratigraphic bodies. Prokop Lim estone sequence. The low est occurrence of the in d e x Pragian tentaculite N ow akia acuaria (typical speci- m en s) is a b o u t 5 0 c m a b o v e th e lo w e r lim it o f th e D vo rc e-

1 1 2 E PISO D ES, Vol. 12, N o. 2, June 1989 D r. W .A . O liver, Jr. is a research 黔 子 CPahluapeoAz6o,1i1c . aondf Ktuhkea l,B Zar.,ra 1n9d8i8a.n P o(sCsaibmlebr gialonb-aMl1ide vdelent sD aenvdo ntihaen s,t rCatziegcrhaophslyo voafk tiah)e. paleontologist with the U .S. G eo- Sbornik geojogic ky ch V ed , v. 4 3, p. 83-146. logical Survey (E-305 N atural H istory Bldg., Sm ithsonian Institu- CKhalrusptA 61,9 I.8,6 I.l aEdxilc,u Jr.si aond LGuukiedse,b oPo.,k ,1 98F6i.e lFdie lCdo Cnofenrfernecnec e,o fB artrhaend iIannt-eMrnoartaivoinaanl tion, W ashington, D .C . 20560). H is Su bcom m issio n on D evo nian Stratig rap hy, 62p., P ra ha. re s e a rc h in t e re st s a re L a te S ilu ria n 愁piaAn6, b oLu,n dLaurkye isn, tPh.e, 1LP oawries}r DFe.v oanidan S ochfb tnhleau Bba,r rHan.Pd.ia, n1 a98re5a. T(Chze cLhocshlokvoavkiaian)-. and D evonian rugose corals and Ja hrbuch d er G eolog isc hen B und esanstalt, v. 128, p. 9-41, W ien. biostratigraphy. He is a past presi- C hlu[)96 . L . Lu kes. P . and W eddilZe , K ., 198 8. C and id ate s for a new Lo chko vian - dent of the Paleontological Soci- PraLian bou nda rv stra to tVp e in the B arrand ian area, C z echoslov akia. M a te rial ety, the Paleontological R esearch sub m itte d to the S ubco m m ission o n D evonian S tratigraphy, R enne s 1988, 1 Ip . Fah rae us, L.E., 197 1. Lo w e r D evo nian co nodo nts fro m th e M ic helle a nd Prong s Institu tio n an d the A m e rica n G e o- C re ek form atio ns, Y uko n T e rrito ry. Jou rn al o f Paleo ntology , v. 4 5, no. 4, logical Institute, and current p . 6 65-683. C ha irm a n o f the S ub co m m ission o n Ja ege r, H ., 1979. D e vo nian G raptolithinia. 竺 ：T h e D evonia n S ystem . Sp ecial D evonian Stratigraphy. Pap ers in P alaeo nto logy, v. 2 3, p . 3 35-339, L ondo n. Johnson, J.G ., K lap per, G . a nd Sand berg , C .A ., 1985. D e vonia n e u s ta tic fluctuations in E uram e rica . G eolog ical So ciety o f A m erica B ulletin, v. 9 6, no. 5, R e f e r e n c e s p. 567-587. K oren, T .N ., 1 979. L ate m o nog rap tid faun as and the problem of graptolite ex tin c- tion. A cta P alaeon to log ica Polo nica, v . 24, n o. 1, p. 79-10 6. A lberti, G .K .B ., 197 9. Z ur D a cryo cona ride n一T en tacu liten) C hrono logie des K lapp er, G . a nd Joh nson, J.G ., 198 0. E nde m ism a nd disp ersal o f D evo nian con o- he rzy nisc hen U nte r- und M ittel-D evons. Se ncken berg ia na letha ea, v. 60, no . 1-3, donts. Jou rna l of Paleontolog y, v. 54, no. 2, p. 400-45 5. p . 2 23- 241. L Utke, F ., 197 9. B iostratigraph ic al sig nifica nce o f the D e vo nian D ae ryo cona rida . A lberti, G .K .B ., 1987. Z u r palNo biogeo grap hisc hen V e rb reltung un te 卜 und In : Th e D e vonian S yste m . S pecial Pape rs in Pa laeo ntolog y, v. 2 3, p. 281-28 9, m itte ld evo nisc her D acryoco narida (T e nta culite n). C ou rier F orschu ngs-in stitu t Lo ndo n. S encke nbe rg, no . 92, p . 161-176. L dtke, F ., 1 985. D evon ia n ten tac ulite s fro m N evada (U .S.A .). C o urier F orsc hungs- A lberti, G .K .B ., 1988. Stratigraph ische U nte rgliede ru ng einige r Lo chko viurn institut Se ncke nbe 馆，no. 7 5, p . 197-226. /P rag ium -G renzp ro file (U nter-D evo n) in N W -M a rok ko, O be rfran ken und Victo ria (S E-A u stra lien) auf G rund von D ae ryoc ona riden and C o nodo nten. S e n c k e n - M artinsson, A . (ed.), 1977. T he Silurian-D evo nian B ounda ry . IU G S Se ries A , n o. 5, be rgla na lethae a, v. 68, no. 5-6, p . 479-493. 349p., S tuttg art. B assett, M .G .,1 98 5. T ow ard s a "com m o n lang uage" in stratig rap hy. Ep iso des, V. 8, M urp hy, M .A ., M atti, J .C . an d W alliser, O .H ., 1981. B io stratig rap勺 a nd evolu tio n no . 2, p . 87 -9 2. of the旦zarkodina remscheiden丝竺Eognatho竺 sulcatus lin即多a }Lower甘兮艺哩色n) in G erm a ny and cen tra l N e vada . J ournal of Pa leontology, v . 55, no. 4, p. 747-77 2. C arts, P ., 198 7. E in V orsc hlag zur biostratig rap hischen R ed efinitio n der G re nze G edinn ium /S iegen iu rn und benac hba rter U nter-Stufe n. E rste r T eil: Stratigraph - Paris, F., 1981. Les Chitinozoaires dans le Pal6ozo-que du sud-ouest de 1'Europe ische A rgu m ente und K orrelation en. C o urie r F orsch ungsinstitut S enck enbe rg, (Cadre g6ologique, Etude syst}m atique, Biostratigraphie). M 6m oires de in Socik 6 n o. 9 2, p . 77-12 1. g6ologique et mi能ralogique de Bretagne, no. 26, 412p. C hlupH , 1. and K ukal, Z ., 198 6. R e flection of po ssible g lob al D evo nian eve nts in W eddige, K., 1987. The low er Pragian boundary (Lower D evonian) based on the the B a rrand ia n a rea, C SS R . L ec tu re N otes in E a rth S cienc es, v. 8, p . 169-17 9, con odon t species E呀 nathod us su lc atu s. S enck enbe rgia na le tha ea, v. 67, G 6tting en. p. 479 -4 87.

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E PLSO D E S, Vol. 12, No. 2, June 1989 113 A N A L Y T IC A L M E T H O D S T H E T E C H N IQ U E S O F A P P L IE D F O R G E O C H E M IC A L M O D E R N S T R U C T U R A L S E D IM E N T O L O G 丫 * }'4 0 1161 ;T A d 191 Z G E O L O G Y R ich ard C. Selley J .C . V an L o on an d R .R . B arefo ot V o lu m es I a n d 2 C O N T E N T S : R o c k to S ed im en t: W ritten for th e p racticin g John G . R am say and W eathering and the Sedim entary analyst, An alytical M ethods for M a rtin I. H u b e r Cycle. Particles, Pores and Perm e- G eoch em ical Exploration ofers ability. Sedim ent Sedim en ted: thoroughly tested chem ical analy- Tran sportation and Sedim entation. sis m ethods for determ ining w hat S edim entary Structures. Environ - base or precious m etals are in geo- m en ts an d F acies. S e dim en t to chem ical exploration sam ples, R ock : T h e S u b su rface E n viron - su ch a s rock s, soil, or sed im en t. m en t. A lloch th on ou s S ed im en ts. Theory is kept to a m inim u m and A u toch th on ou s S ed im en ts. S ed i- com plete procedures are provided m entary B asins. E ach chapter in- so th at n o ad dition al sou rces are clu d es referen ces. in d ex . needed to conduct analyses. In Paperback: $34.00 1988, 344 pages, $49.95 IS B N : 0 -12 -6 36 3 66 -8 IS B N : 0 - 12 -7 14 1 7 0 -7 C aseb ou n d : $ 79 .50 IS B N : 0 -12 -6 36 36 5 -X 七我签挺盛翔寿幻盘挑慧沈艺甜 爱昆迸瑟蕊续夔 盗登盔 慈建地维 198 8 , 4 46 pages B A S IN A N A L Y S IS Q u a n tita tiv e M e th o d s V o lu m e 1 Ia n L e rc h e In Paperback : $29.95 IS O T O P E T h is is th e first b ook in its fi eld IS B N : 0-12 -57 69 2 1-0 C H R O N O S T R A T IG R A P H Y to d eal w ith th e qu an titative as- C aseb ou n d : $6 9 .0 0 T h e ory a n d M e th o d s pects, u n certa in ties, a n d resolu - IS B N :O - 12 -57 69 0 1-6 tion lim its of basin analysis. The 19 84 , 3 2 4 p ages D ouglas F . W illiam s, Ian Lerch e, p u rp ose of th is volu m e is to in te- an d W .E . F u ll grate know ledge of the dynam ical, V o lu m e 2 th erm al an d h yd roca rbon h istories In Paperback: $35.00 This is the fir s t title to bring to- of sedim ents and fluids through IS B N : 0 -12 -5 76 92 2 -9 geth er the latest data and quantita- geologic tim es using quan titative C a seb ou n d : $ 84 .00 tive m ethods of isotope chronostra- m eth od s. T h e em p h asis is on th e IS B N : 0 -12 -5 76 90 2 -4 tigraphy and signal processing, a u n c e rta in tie s a n d re so lu tio n lim its 19 8 7 , 4 07 pages rapidly developing area of research. of basin analysis given con straints D esigned to fam iliarize petroleum d erived from su rface an d d ow n h ole geologists and stratigraphers w ith d ata a n d th e sen sitivity to m od el 越潇势公岂蜡吐越遨生出猫婆塞继理竖器老骂得鳄粼攀忿签过舀盔 this new form of chem ical stratig- in p u t p aram eters a n d assu m p - Now available in p aperback! raphy, the au thors attem pt to show tio n s . th e potential of using stable oxygen F R A C T U R E M E C H A N IC S and carbon isotope records for Novem ber 1989, c. 476 pages O F R O C K m aking detailed stratigraphic cor- $8 9 .50 (ten tative) relations of exploration sections of IS B N : 0 -1 2 -4 4 4 17 2 -6 edited by B arry K e an A tk in so n T ertiary and M esozoic ages. 1988, 345 pages, $49.95 Paperback R eprint: $39.95 IS B N : 0 -12 -75 45 60 -3 IS B N : 0 - 12 -0 6 6 2 6 6 -3 19 89 , 534 p ages C aseb ou n d : $ 129 .00 IS B N : 0 - 12 -0 6 6 2 6 5 -5 198 7 , 5 34 pages a A C A D E M IC P R E S S — H arcourt Brace lovanovich, Publishers B ook M arketin g D epartm ent #2 1069 , 1250 Sixth A venu e, S an D iego, CA 92 10 1 C A L L T O L L F R E E i-s oo -32 i -5o bs C 1989 by A cadem ic Press, Inc. All Rights Reserved P rices s ub ject to ch ang e w itho ut no tice. D K / ES #21069

114 E PISO D ES, Vol. 12, N o. 2, June 1989