Late Devonian-Carboniferous Conodonts from Eastern Iran

Rivrsta Italiana di Paleontologia e Stratigrafia volume lul numero 2 tavole 1-13 pagrne 167-200 Setternbre 1999

LATE DEVONIAN-CARBONIFEROUS CONODONTS FROM EASTERN IRAN

MEHDI YAZDI*

Receioed December 10, 1998, accepted May 24, 1999

Key-uorcls : Conodonts, biostratigraphy, Shotori Range, Howz- interval of siliceous sand ("the white quanzite" of previous aurhors). e-Dorah, Kale Sardar, Bahram Formation, Shishtu Formation, Sardar Additionally, several iron-rich horizons, readily traceable from locali- Formation, Frasnian, Famennian, Tournaisian, Visean, Namurian, ty to locality, are well constrained by conodont ages. tVestphaìian. Eighty-five conodont species,/subspecies are documenred representing 24 genera. Two new specres, PoLygnathus capollochì and Riassunto. Vengono presentati i risultati del trattamento di 110 Polygnathus ratebi a,nd one new subspecies, Icriodus alternatus ntauso- campionì per ccìnodonti provenienti da due sezioni di Devoniano su- nae are described. periore - Carbonifero nella Shotori Range in Iran orientale (regione di Taba$. La successione di Howz-e-Dorah, (con 88 campioni) inizia nella pane alta della Formazione Barham (Givetian-Frasniano inferio- Introduction. re), prosegue attraverso la Formazione Shishtu (dal Frasniano, Zona a hassi, srno al Tournesiano terminale, Zona a anchoraLis-latu) e la For- Reconnaissance invesrigations of the Shotori Ran- rnazione Sardar (dal Viseano basale, Zona a texdnus, sino alla Zona a ge in eastern Iran (e.g. Stócklin et al. i"965, 1991) de- sinuatus-corrugatus-sulcatus) per concludersi nella Formazione Jamal monstrated existence del Permiano. Altre 4 sezioni stratigrafiche, campionate in modo the of an excellent Late Devonian- meno esàustivo (22 campionl) indicano che I'area di Kale Sardar è pirì Carboniferous succession in the Tabas region (Fig t) complicata tettonicamente della zona di Howz-e-Dorah. There has been very little previous palaeontologic work lJtili onzzontr guidr della sezione FIowz-e-Dorah, ben calibra- in the area; nothing of signi{icance has been published ri dai conodonti sono rrsuitrri i teguenti: on the diverse macrofaunas during the years 1) i brnchi biostromali della Formazione Shishtu, non pi,! an- past 30 but tichi della Zona a hassi inferiore, 2) un intervallo di calcari oolitici older publications include work on Devonian and -ùTalliser del Famenniano inferiore (Zona a trianguLaris aLta o crepida infelo- lower Carboniferous goniatites by (1.966), re), 3) una sequenza cicloternica che passa attraverso il limite Carbo- Frasnian rhynchonellid brachiopods by Sarrenaer (1966), nifero inferiore - Carbonifero superiore, ed infine 4) un intervallo di Iranoblastus, a new Eariy Carboniferous E. uenarie silicee (a "white quanzite" degli Autori), riferibile al Per- blastoid by miano ìnferiore. Inoltre, diversi orizzonti ferriferi, facilmente correla- Flùgel (1966) and Receptaculites by H. Fiùgel (1961). bili, sono ben calibrati mediante le età a conodonti. Sono identifica- \fleddige's (1984) more recent conodont srudies concen- te 85 specie di conodonti, che rappresentano 24 generi. Infine sono trated on faunas to the north of the area presently un- descritte 2 nuove specie, Polygnatbus capolLocki e Polygnathus ratebi, der consideration. In order ro address this deficiency, ed una nuova sottospecie, Icriodus ahernatus md@sonae. sections aggregating 1360 m were sampled for cono- Abstract. Conodont data from acidJeaching 110 samples from donts in the Howz-e-Dorah area (Fig. 2, 4) and in the rwo Late Devonian-Carboniferous areas (Tabas in the Shotori Range vicinity of Kale Sardar (Fig 3) with the aim of estab- region) of eastern lran are presented. At F{owz-e-Dorah, a secrion (88 lishing a stratigraphic framework other sarnples) commencing high in the Bahram Formation (Givetian-early within which Frasnian) extended through the Shishtu Forrnation (Frasnian, Early faunal groups (for example, ammonoid and nautiloid ce- bassi Zone or oider, to latest Tournaisian, anchoraLis-latus Zone) and phalopods, brachiopods and mollusks) will be able to be tlre Sardar Formation (earliest Yisetn, texanus Zone, to late Namu- accurately located and bioevents and transgression-re- rìtn, sinuatus-corrugatus-sulcatus Zone) and into the Formation Jamal gression patterns compared with others elsewhere (Permran). Four less exhaustively sampled sections (22 samples) show the Kale Sardar area to be tectonicxlly more complicated than the (Yazdi, 1.999, in press). F{owz-e-Dorah area. Useful marker horizons in the Howz-e-Dorah The revised Late Devonian zoîal scheme oÍ Zre- section, well constrained by conodont data, are: the eady Frasnian gler 6c Sandberg (1.984, 1990) is used herein; in some (no older than Early hassi Zone) biostromal beds of the Shishtu For- instances, for clarity, aiongside the zone quoted, appears, mation, an early Famennian (Ltte triangularzs to Early crepida) ìnter- val of oolitic limestone, a cyclothem sequence straddling the Early in square brackets, the original zonal equivalent (sensw Carbonìferous-Late Carboniferous boundary, and an Early Permian Ziegler 1962, 197I), eg. Early rbenana Zone l: Lower

'r Centre of Ecostratigraphy and Palaeobiology, Macquarie University, 2109, NS\í, Australia, and Depanment of Geology, Faculty of Science, University of Esfahan. Isfahan. Iran. i68 M. Yazdi

gigas Zonef. The Carboniferous zonal scheme used throughout is based on the oritcomes of the Carbonife- rous Subcommission Meeting, Provo, lJtah, 1988 (Brenckle & Manger, 1991). Conodont genera mentioned in the text and on Tables 1,,2 and 3 are abbreviated as foliows: Ad. :Ancyrodella; Alt. :Alternognatbus; An. :Anry- rognathus; Cl.--Clydagnathus; D.:Declinognathodus; Do.-Dollymae; Gn.:Gnathodus; L:Icriodus; Id,:Idio- gnath odws ; L. : Lo chriea. N g. : l"l eognathodus ; P. : Po lygna- th us ; Po. : Po ly I opb odo nta ; Pa l. : Palntato I ep is ; Pel. : Peleky - s gndtb us ; Ps. : Pseudopo lygnathus ; Rb. : Rhach istognatbus ; Sc. :Scaliognathws; S. : Scaphignatbus; Si. : Siphonodella.

Previous work.

Reference to the geology of the Shotori Range in the Tabas area in eastern Iran was first made by Sven Hedin (1927), who, during his expedition to Central Asia some 20 years earlier, named the prominent moun- tain, Kuh-e-Shotori and collected an Early Jurassrc sedimentary sequence at its base. Late Palaeozoic limestones were reported by Furon (1941) from the ranges east and west of Tabas and in 1951 Gansser climbed Kuh-e-Sho- tori; he was the first geologist to do so. Gansser (1955) gives a brief account of Carboniferous shales, Triassic dolomites and red shaies and Late Jurassic reefal limestones of the area. Stòck1in (1961) reported the first De- vonian cephaiopods from Iran. The first systematic investigation of the area, undertaken under the auspices of

the Geological Survey of lran, was carried out by J. Stócklin, J. Eftekhar-Nezhad and A. Hushmand-Zadeh vzith the assistance of M. Nabavi, M. Zahedi, N. Valeh S. Tatavussian; their findings are summarised in Stòc- klin er al. (1965, 1991). The study was comprehensive covering the geoiogy of the Precambrian to the Quater- nary.

Geological setting.

Stòcklin et al. (1965) named three pre-Permian formations of the Ozbak-Kuh Group: the Bahram For- mation, the Shishtu Formation and the Sardar Forma- tion; the Permian sequence lying above these was named the Jamal Formation. The Sardar conglomerate was thought to have lain unconformably between the Shishtu and Sardar formations. The sedimentary sequence of the Shotori Range is characterised by numerous hiatuses, unconformities and

Fie 1 Geology of the Shotori Range in the vicinity of Tabas, eastern Iran simplified from Stóckln et al. (lleS) with mi nor modifications from subsequenr f,raverses. DetLonian-Carboniferous Conodonts from lran 169

Fig. 2 - F{owz-e-Dorah area showing simplified geology and the location of the Howz-e-Dorah section, A to A1 synsedimentary faults. The type sections for the Shishtu It is located between Howz-e-Mohammad Ghasem Formation and Sardar Formation selected by Stócklin er and Sorond village, approximately 75 km southeast of al.. (1965, p. L1.-19) at Flowz-e-Dorah and the Sardar Ri Tabas (Fig. 1, 2). The base of the section commences ver area are interruprcd by a number of hiatuses and 700 m northwest of Howz-e-Dorah at the boundary be- locally show changes in thickness. For this study a more tween the Bahram Formation and Shishtu Formation complete section passing through both formations was and continues through the Sardar Formation to the Ja- sought. The section seiected is approximately 2.5 km to mal Formation (Permian). Limestone horizons were the north of the section documented by Stócklín et al. sampled for conodonts and macrofauna along the sec- (1965) at Howz-E-Dorah (Fig. 2, 4). It commences in tion line. the topmost horizon of the Bahram Formation (Early Frasnian), passes through the Shishtu Formation 1. Shishtu Formation. the Sar- (Frasnian, Famennian anóEarly Carboniferous), The lowest horizon of the Shishtu Formation (A- Sardar dar Formation (Carboniferous), including the A1 on Fig. 2, 4) occurs above a brown, siliceous dolomi- conglomerate (post Namurian) and into the Jamal For- tic horizon that marks the top of the Bahram Forma- conti- mation (Early Permian). The Jamal Formation tion. A second locality in the Shotori Range where the nues into the Late Permian (Figs. 2, 4, 5). At Kale Sar- Bahram Formation crops out and the base of the dar a number of short sections (Figs. 3, 6) have been Shishtu Formation is exposed is in the vicinity of the Howz-e-Dorah coilected to supplement data from the area approximately 2 km northwest of Howz-e-Moham- section. mad Ghasem on the Tabas-Kerman road, about 80 km southeast of the city of Tabas; here the top of the and base the Shishtu Forma- A. Howz-E-Dorah Section (Fig. Z). Bahram Formation the of tion are not clear. Co-ordinates for base of sec'tion: Long" o22'50"N. 57 2A' 28"8, Lat. 33 " 2. Shishtu Formation and Sardar Formation Boundary" Co-ordinates of top of section: Long. 57"20'45"E, Lat. 33"23'15"N. The boundary between the Shishtu Formation (: (From Deh-e-Shahzadeh'Ali 1:50,000 Iran sheet, top of Shishtu 2 of StóckLn et dl. 1965, 1'991, p. 1'8'2A) Ni-40-1t 0456r) K753. and the Sardar Formation occurs between a 2-3 m hori- 17a M. Yazdi

4. Permian.

The Jamal Formation as defined by Stócklìn et aÌ. (1.965, p. 2t-22) consists of from 500 m to 8OO m of Permian sediments. Not included in the formation as originaily defined is a white unit of siliceous sand, the result of a transgressive event at the base of the Per- mian. Partow Azar (1992) included this sequence within the Permian naming it the Baghe Vang Member. This siliciclastic sequence is thought to be related to the posr- glacial event of Gondwana (Husseini, 1,992, p. 423).The siliceous sand, commonly referred to as "white quartzite", varies in thickness from 40 m to 60 m, and clearly overiies the uppermost horizons of the Carboniferous. Contrary to Stòcklin et al. (1965, p. 20), the unit is not part of a continuous sedimentary sequence as conodonts have shown there to be a substantial gap in the sequence coinciding with the upper part of the Late Carbonife- rous (see discussion below).

B. Sections at Kale Sardar (F;g. 3, e).

The Kale Sardar area is located 25-28 km east of Tabas, in the foothills of the Shotori Range (Fig. 1) in an area of severai northwest-southeast trending Late Pa- laeozoic and Mesozoic sedimentary sequences (Fig. 3). Palaeogene and Neogene-Quaternary volcanic sediments cover the topographicaily lower areas. In order to supplement information gieaned from the study of the Howz-e-Dorah section, four additional sections were sampled at Kale Sardar. Of especial inte- rest was the Sardar conglomerate; limestone clasts collec- .were ted from the conglomerate individually processed for conodonts in order to obtain a minimum age the Fig. 3 - Kale Sadar area showing simplified geology and location of for the Niaz section, Section A, Section B and Section C. date of its deposition. Stratigraphic information obtai- ned in the vicinity of Kale Sardar will assist in the eluci- zon of sandy crinoidal limestone grading to a muddy, dation of the structural complexities of the area. sandy limestone with an influx of fine sediment and a coarse-grained sandy horizon, the base of which is 1. NIAZ section (Fig. 3, 6). rough and uneven suggesting a possible erosional event. Co-ordinates for base of the section: I-ong. Stòcklin et al. (1965 p. 18-20) repofted that a conglome- 57o8'18'E, Lat. 33'39'30"N. Formation, at ratic sequence overlies the Shishtu but Based on Khan-e-Pain 1:50,000 sheer, Iran. F{owz-e-Dorah this is represented by a coarse-grained 7457111. K753. sandstone that grades into a sandstone horizon contai- The age of the Sardar conglomerate at Niaz viila- ning small, rounded cherty pebbles. ge, thought by Stócklin et al. (1,965, 1,991, p. 16, 56) to represent an unconformity between the Shishtu and Sar- 3. Sardar Formation. dar formations and, accordingiy, argued by them to be Stòcklin et al. (1965, p. 16) in choosing the type Early Carboniferous in age, is shown herein to be no section for the Sardar Formation, a locality south of the older than sinuatws-corrugatus-sulcatus Zone (early Late Sardar River at Kale Sardar, stated that "this is not an Carboniferous, Namurian). ideal section because the lowermost part of the Forma- Stócklin et al. (1.965, 1991., p. 56) suggested that tion and its contact with older rocks is not exposed". the Sardar conglomerate resulted from epeirogenetic mo- The section at FIowz-e-Dorah described herein provides vements commencing in the Late Devonian and conti- a more complete record of the Sardar Formation than nuing into the Permian. The presence of more than 20 the type section. m of Sardar conglomerate at Kale Sardar (Fig. 6) indica- Deoonian-Carboniferous Conodonts from Iran L7 1,

A. 2100 ,^r^r,Í:ÀÎ^îtt? .-- 2000 sar d2:.::í#Í,i'on ."..0u,. (t": Conglomerate 1 900 equrvalent C) c) (g 1 800 oc) c)

(ú 1 700 o 0) A ()

1 600 E

1 500

1 400 500m

Fio 4 Diagrammatic geological section of the Howz-e-Dorah section, A to A1, indicating the approximate boundarìes of the Shishtu Formation, the Sardar Formation and the Jamal Formation. See Fig. 2 for location of section . tes that the structural history of the Kale Sardar area the shales appear to correlate with those of the Sardar differs from that of the Howz-e-Dorah area where it is Formation cropping out around 590 m to 730 m in the represented by an erosional surface (Fig. 5). Flowz-e-Dorah section.

2. Section A, 2 km NW from Tang-e-Abbasi, near Tabas 3. Section B, at Kale Sardar, near Tabas (Fig. 3, 6). (Fig. 6). 3, Co-ordinates for base of the section: I-ons^ Co-ordinates for base of the section: Irrns, 57 "7' 40' E, Lat. 33'39' 15 "N. 57"7' Q'E, Lat. 33"40'30"N. Based on Kharv-e-Pain 1:50,000 sheet, Iran. Based on Kharv-e-Pain 1:50,000 sheet, Iran. 7457rrr, K753. / +)/ IL r\/ )J. The section (Fig :) commences in a green, sandy The section (Fig. 3) commences with a series of shale and muddy sandstone sequence. Although there is oolitic limestones alternating with muddy limestones no apparent erosionai surface at the top of the shale- containing cephalopods. From 11 m the fossiliferous sandstone sequence, there may be some loss of section iimestones become red to brown in colour. Conodonts at this point as the ensuing series of three horizons have from sample 6, at 15 m, are consistent with an Early or their equivaient in the F{owz-e-Dorah section whereas Middle expansa age (Famennian, Late Devonian). The the shale-sandstone sequence is not represented in the horizon can be correlated with the interwal from 339 m more complete section to 343 m in the FIowz-e-Dorah section, both having a From 37 m, thin-bedded limestones alternate with similarly high number of cephalopods and other macro- colour-banded horizons of striped chert. From sample 14 fauna including species of orthoceratids, goniatites, and at 38 m, conodonts indicative of the anchoralisJatus Zone gastropods in common. (ate Tournaisian, Early Carboniferous) were recovered. sequence can correlated with that from 510 m to At 19 m there is an erosional surface after which This be 550 m above the base of the section at at Flos/z-e-Dorah. the limestone becomes white with some nodular horizons and an occasional grey or green shaley limestone 4. at Kale Sardar, near Tabas (Fig. 3, 6). bed. A fauna of the Frasnian (Late Devonian) species, Section C, Beloceras tenuistriaturn from nodules at 21 m indicates Co-ordinates for base of the section: I-ons. o39'8 surface 19 m marks a fault bound- 57 30" E, Lat. 33 "N. that the erosional ^t "7' ary. At 37 m, the sequence again changes abruptly rc a Based on Kharv-e-Pain 1:50,000 sheet, Iran. series of green shales and sandy shales. Lithoiogically, 7457111, K753. M. Yazdi

a) N .e

co o N = oQ 480_ 23 o 527 s

506 460_ 10 505

440_

680_ cC) N q) $ a) 525 Nì c 660_ c $ 21 _ o #,, fi', E c F (ú .9 (u 524 (! N E E *, :ljil:. 20_ E tL s u- r 523 LL 0 f t::/t',, = (ú c .9 64Q_ .o c= (g c 19_ a a a 522-

521 _

620_ 520 -

18 _ 28 51 g'

518 , 600_ 517 516

q) c 515 N a) $ a)

(! 320. (!c E 502

o) 501 ó 300_

28q 12 Jq,:É

260 Deponian-Carboniferows Conodonts from Iran 173

1100 m- c E Nj .. ::fr: LL #: ,4' (g iK E ,l\ (ú 4:':,;/.r, ftt: c ,f,i{i: iil:i 108L - .Go f c.j G C) o c c - .E(g N (ú 5 -?- c c 1 060 q) F .g 6 (ú (d è. c IE c! f 980_ A2 (g q) .a = c (ú a c A1 t c N o É (ú (ú 1 040 o o - o@ = o c N 1 020

ffi Alternation of thick to massive limestone with ffilf;r-ir;Ìl brachiopods and macro fauna including corals and crinoids

t-r:==ffi Thick to platey grey to brown limestone with striped ffi beds of chert with brachiopods,crinoids, bivalves, gastropods, corals & rarely cephalopods

Alternation of ash grey to black thick bedded Fri?ì-r[?Tl limestone with solitary corals, brachiopods, crinoids, trilobites and bivalves FFil#t Sandy fossiliferous limestone c |TffiE=Ti]H E (ú c E (ú 880_ t-77= Yellow to brown sandy dolomite intefingering with IL f rrl.t4 limestone; some localities with crushed and c 6 zG scattered crinoid remains (ú ct) ffi Yellow to pink, dark brown, oolitic sandy limestone rYfsl with brachiopods, bivalves, ostracodes, hyoliths, but sparse conodonts

|- Alternation of thìn-bedded green to grey limestone, marly green limestone with brachiopods

fE-...\-li]I]\]l Grey to white sandstone, coarse grained at base, [ ::: :!::]t::t. ::t :1 J:r::1iq+!ì changing into conglomerate locally

Sandy shale with brown to purple sandy nodules 39 - --l 820_ 534 532 Conglomerate with semi rounded boulders o Ei;;;È-.gffi (including megaclasts) of diverse lithologies C including limestone and dolomite N E--EÍAflm White, coarse to medium grained cross-bedded ! quartzitic sandstone q)a li.ii,t\l:$';::ii:i*,ì È o Grey to blue sandy shale wilh cone-in-cone structure 6 ffi Yellow dolornite

fYr---t vl F:-:--l Gypsiferous grey to black sandy shale 780 38 -

Stratigrephic section at Howz-e-Dorah. As the section was sampled on 3 occasions (in 1991, 7992 and 1.994), each series of samples were numbered independently. The 3 series o{ sample numbers appearing adjacent to the section column rre printed in 3 font sizes to differentiate the 3 collectrons. M. Yazdi

Frc É, - (t r.rr rcrrnhic ."ct ions rt Krle Sardar: Niez, Section A, Sec- tron B, Sectron C. For le- c gend see Fig. 5; for locality c F of sections see Fig. 3. 6 E 18 E l '17 E L z6 16 6 85 conodont species,/subspecies ! 6 tc a(Ú o (Tables 1-3, Plates 1-13) and a

14 number of macrofauna collected from the Shotori Range. For the Late Devonian, the most commonly accepted conodont zona-

c tion is based on the distribution F 6 c. of the pelagic species Palmatole- E C o .6 pts (Zteg\er & Sandberg, 1990). I c @ 6 According to Sandberg 6c Dree- ! l! _@ o5 c. sen (1984, p. 150) and Savoy & Section B Harris (1,993, p. 2416) PaLmato- at Kale Sardar leprs species lived mostly in a pelagic and basin habitat. That c c .g rare lo c species of Palmatolepis are :62a d in the Late Devonian of the I DOI Range indicates that Fam Shotori most of the sediments of the area may have been deposited in Section at Niaz shallow water. It should be no- ted, however, that although pal- rnatolepids are not common in c F 50_ rn L rhe Shotori Range sections, attempt has been made to tie È 40_

M€l€6 above base ofsection 54 83.5 181 191 195 205 202 220 231 279 292 291 298 310 313 3'18 33S 343 345

Sampìe number 503 504 I 505 10 506 't02 11 507 508 509 510 Gha-Ka 12 51'1 512 513 't03 15 514 515 16 7 516

2 3 3 3 4 .o,,ooJJÉ 4 4 4 4 4 4 filltnilhus ùrD(lundi Pa x ['. rapollocki n. sp. Pa 1231 34 121 lcfiodus allemútus ultenrutus Pa 112't1 I alte nutils moah lî Pa 62311227167 1 sD.B Pa 1 ,4ncyradella nodoso Pa 112 P erùíen.t Pa 1311'1 1 2

I rrpdiilt! Fa 1 I cî.1. irt*oensit I 'J Pa

sb 1

P aeoualì.r Pa 2

P. i,chbi Pa 1 2 pk|tarhd P Pa 2 5 '1 3 P aîf.l'. ons.ttitli.tcus Pa 21 2 l'. btn'icarhw Pa 43

í torraen.e$ iov,aeù:is Pa 1 23 1 I aîf. L tor'acnsis iotruen;ts Ca 2

Ancyrognaùu: sielantìila Pa 2 ?1 cf. f. acillatils Pa 2 3 connlilt Pa 2 P(hk\rp^illtt\ h^lDtutxî Pr

I' c[. oaoìlok! Pa 1 olt|n)útù.r ùrNtoùac \rh.r P^ ^ '15 .î. I sp. L cohrylu$ Pa ^fl. 22 I' ruh.tt \1.sD. I, I l'.nsDA Pa 1 l\l|tatalrDir il'hnùa ùtilùto Pà 1 lill qtrilfuilttnlodos1lohqtu Pa 1 I'ul. \thDcrhl\ttu Pa 2 P 5 l ,'l c{ rttttrrttrtrt Pr 3 I' cililtnltnt\ Ltilililtùilt\ lJî 11311 lu 1 6 1 15 I .otiltil\ durltr(,ttt\ tlr 10 i'lthltlilt sDp. Pa 221 I trl, \tt\ Pî r', 6 1' Ìì so. Il Ìta 1 /i,/ su C l.l 1 cl. crpcrplt.tus I,î 1 ( Ir,Lt\txilhil\ "ililtkilil Pr 31 )'olrloolulotta Lonfntnr l':l 1 Unassigned elamerls 1 5 33 3 6 5 5 72 80 10 17 12 60 E4 12 16 17 3 456 I 37 35 50

Tab. 1 - Distribution of conodont elements from the Howz-e-Dorah section (A-.A1) for the Devonian ponion of the Shishtu Formation.

Sartenaer (1966) and dated broadly as Frasnian. On the 3. jamieae Zone. basis of conodont data, the fauna can now be restricted Based on ranges suggested by Klapper (1997), tbe to the lower half of the Frasnian, late Early hassi Zone occurrence o{ Ad. nodosa, P. et-tidens and L alternatus al- or older" ternatus,114 m above the base of the section are consistent with an age of. jamieae Zone. 2. Late Early hassi Zone. Note: Apart from rhe occurrence of dolomite beds at various levels, the section from the commence- Eighty four merres above the base of the Howz-e- ment of the jamieae Zone appears to be continuous. Co- Dorah section, the incoming of Polygnaihus aspelundi nodont data available for the nexr 195 m of section do suggests that this level is no older than late in the Early not allow the various zones from Early rhenana (: hassi Zone and is no younger than jamieae Zone. This is Lower gigas Zone) to Early niangularis (: immediately based on the age and range P. aspelundi of given by above the Frasnian-Famennian boundary) to be clearly Klapper (1997). In their discussion of the zonation of defined. Conodonts occurring within this interval inclu- the Lali Section, South Ziegler (1993, China,li tt p. 18, de: Icriodus alternatus alternatus, L expansus, I. cf. L io- 19) include P aspelundi in their discussion of the puncu- waensis iowaensis, Polygnathus aequalis, P aff . P. angusti- ta Zone, grouping beds 21-28 from the Lali secrion in discus, P, breoicarina, P. er,,ìdens, P planarius, P capollocki this zone. In the description of the individuai beds of n. sp. and P webbi. At 205 m above the base of the the Lali Section, however, Jt tr Zíegler (1993, p. 12) section, P webbi and a single specimen of an orthocera- show that P aspelundi firsr occurs within Bed 25 sugge- tid were recovered. The bed also contained a Frasnian sting the possibility that this bed could represent the brachiopod fauna identified by Sarrenaer (in Stócklin er commencement of the Early bassi Zone. al., 1991, p. 12) that included: Hypoilryridina c{. cuboides 176 M. Yazdi

Met€rs above base of sectron l4ì 348 351 359 361 368 389 398 399 400 405 41t 511 ;54 t6l 571 584 609 646 706 71 711 712 718 /21 745 824 t8;

Sample number 51 104 51t 519 18 520 52 52:. t9 105 523 20 524 521 22 i2f 2! 53i 106 29 33 ;3. 34 147 533 35 36 108 109

4 4 4 4 4 4 4 4 4 4 4 4 ."-ìt Polygnathus inornatus Pa 13682

Pa 11 1 12 121 I P- communis conmunis Pa 2121 18 6 3 Siphonodella ìsostìcha Pe 3 .Si. cf. obso/ela Pa 2

PseudÒpolygnathusmúltislrìatus Pa 12611 ',X cf ldbpnonodus sp. Pa 22212 Pa 1 Ps. pinnatus Pa ?1 1 Gnalhodus delicatus Pa

Gn. semiglabeÍ Pa 14111 112 Gn. typicus Pa Gn pseudosemtglaber Pa Gn. gitiyi gitfyi Pa 11236143 ldiapioniodus ssp. P 2103 Gn. giì1yi intermdius Pa 1 13 4 Gn. gitlyí simplex Pa 14?211s ldiognathaides sp. Pa 1 Lochdea commutata Pa 6 3

Pa 12 ldiognathadus sinualus Pa 4 NeognathodÌs cL medadultiúus Pa 2 Neoqandolella cf. clarki Pa lness oned elements 318930 10 7 1 7 1 6 7 72 39 69 191416 7 27 2 2 13 I 93 4 15 414324 9 31 4s

1f,D.1 Distrìbution of conodont elements from the Howz-e-Dorah section (A--A1) for the Carboniferous portion of the Shishtu Fonnation, the Sardar Formation and the lowermost famal Formation (Permian)'

(Sowerby), Schizopboria cf. s*iatula (Schlotheim), Srro- pIe7,1.8 m above the base of the section [: top of bed pbonella sp., Atrjpa cf. reticwlaris (Linné), Strophonella 12 of Stócklin et a\.,1991, p.151 have been identified by c{. productoides (Murchison), Cyrtospirifer of the group Prof. M. FIouse as: Beloceras tenwistriatum var. nov. oerneuili (Murchison), and Atbyrk cf. commwnis (Gosse- (pers. commun., June 1995). This is the first report of let)" Because of the constraints of the conodont fauna, a this species from the Shotori Range. As Ad. curaata late late Frasnian age (no older than jamieae Zone) can now form and Pal. uinchelll were recovered from the same be attriburcd to this fauna. horizon (Table 3), Beloceras tenuistriatum at Kale Sardar can not be younger than late Frasnian ffrom Late rhena' 4. Iinguiformis Zone (?Frasnian-Famennian boundary). na Zone to the end of the lingutformis Zone). At Kale Sardar, the white, sandy oolitic limestone varies in thic- At 279 m above the base of the Flowz-e-Dorah kness from outcrop to outcrop and at times intertongues section, the last occurrence oÍ AncTrodella cuntata late with green shale" This is contrary to Stócklin er a/. form and Ad. nodosa suggests a level close to the top of (1.991., p. 16-18) who documented all green shales as be- the lingutformis Zone. Ziegler & Sandberg (1990) sug- longing to the Sardar Formation and dated as Late Car- gest both these species became extinct at the end of boniferous in age. As outlined above, conodonts inter- Frasnian. The last element related to the Ad. curuata late preted as Late Frasnian in age. sugBest a date for at least form from sample 12, 279 m above the base of the sec- portion of the green shales that inter-tongue with the tion came from a limey white to brown sandstone bed white, sandy oolitic limestones. from vzithin a sandy sequence below a sequence of beds rich in cephalopods, referred to by Stócklin et al. (1965, 5. Late triangularis Zone or Early crepida Zone. 1991) and herein as the "Cephalopod beds". Although the dark rich shales usually associated with the Kellwas- At 291 m above the base of the Howz-e-Dorah ser Event are not represented in the Howz-e-Dorah sec- section, a series of red, richly fossiliferous, sometimes tion, the bed containing Ad. curaata within the sandy oolitic limestones commence. These beds, as mentioned sequence may possibly be correlated with the Kellwasser above, are generally referred to as the "Cephalopod Event found elsewhere globally. The Frasnian/Famen- beds". The basal bed, sample 13, a red sandy oolitic nian boundary may have occurred with within sample limestone, normally indicative of well oxygenated warm 12,279 m above the base of the section' or very close to water, yielded no conodonts possibly because of the this level. high oolitic content. FIowever, as the macrofauna and Cephalopod specimens collected from a white san- vertebrate microremains from the sample have either dy oolitic limestone at Kale Sardar (Niaz section, sam- been changed to or are covered by chamosite, the envi- Deponian-Carboniferous Conodonts from lran 177

Tab.3 - Distribution of conodont Section NIAZ B elements from sections ìn SrmDle number 1 2 3 5 I 1C 11 o 8 14 15 1/ the Kale Sardar area: Niaz o Section, Section A and Sec- Meters above base ofsecîion q o di Ni N tion B. ------Samplewt. (kgì ------Conodont taxa Famennian Icriodus alternatrc s.s Pa Early Palmatolepk I. allernatus alternalils Pa 11 31 crepida Zone" . Alternatively, it f. cî. L alternatus Pa L cf I all L cornutus Pa could dated as Middle or Late L expansus Pa 6 trzangularís Zone as, apaft from Icriodus sD. A Pa Pa P. acutatus, the associated fauna Idioprronotds ssg. Pa 5 cf. ldrcprionoids so. Pa 5 are rePresented in these zones. Scaliognathusanchoraliseuropensís Pa 6 At 313 m above the base Anclrodella cumata Pa 67 Ad. nodosa Pa 1 oI the FIowz-e-Dorah section, BísDathodus stabilis Pa sample 103, Lochriea comhutdta Pa in the numbers of MPhlika sD. l)a icriodontids represented in the Pseudopolvznathus conlroversus Pa ?1 Ll I's. triungularis tnequalis Ia fauna increases rapidly also indi- Ps. pinnatus Pa cative of very shallow water. A Pa Sc. velifer leptus Pa 4 kg sample yielded more than

Polyznqthus conmunis coùmunis Pa 1 200 conodont eìements and ap- P. conmunis collinsoni Pa 2 P. evídeks Pa proximately 900 vertebrate mi- P- longiposticus Pa P- nodocostaîus Pa '1 cro remains. Pa 1 This time interval is also P. oerplexus Pa 1 P. nlnnariltî I)a recognised at Kale Sardar where P. senticostatus Pa 1 cl P. rvmmelricus Pa 2 a clast from the Sardar conglo- P tapolloc*i n sp t merate, sample 11, yielded a si- P. n. sn. A Pa cf P. uncolnis Pa milar {auna. Important species P. webbi Pa represented in the Shishru For- Pal|úloleDis glabra pectinata Pa Pdl. kapperì Pa mation af both localities for Pal. ilinuta miiluta Pa M this time interval include: Icrio- Pal.:ehindwolfi Pa dus alternatus alternatus, I. cf. L Pal. perlobata siemoida Pa Pal. quadrantinodotalobata Pa sp. îff. l. cornutus, L iozuaensis Pal sn. A Pa iowaensis, Polygnathus cf . P papi- Pal. so. B Pa Pal. sp D Pa lata, P ratebi n. sp. P n. sp. ,4, c[. Pul. vinchelli Pa Pal. wolskae Pb Palmatolepis minutd minuta, Pal. 4lîcrognulhadils so Pa quadrantinodosolobata, Pal. sub- Cúathodus pseudo-tentiglaber Pa 61 5 10 3412 Gn. senìslaber Pa 12 perlohata, Pal. tenutpunctata, Gn. Noicus Pa 51 1 '1 5 and Pal. cf. tenwipunctata. Gn. bilineatus Pa 1

CnathoJus so la 1 Declinosnathodus noduliferous Pa 7 ldiopnathoidcs sinualus Pa 3 6. Middle crepida Zone.

Hindcodelta scqaformts Pa 1 Unassiened elements t25 24 16 7 ts4 6 t0 l0 lt 8 65 134 l On the age attributed to P. semicostatus by Dreesen & ronment must have been one of a restricted area where Dusar (1974), the incoming of this species in sample reducing conditions could be combined with periodic 515, 335 m above the base of the FIowz-e-Dorah sec- rough water conditions as suggested by Odin (1988, p. tion, indicates an age no older than Middle crepida 2a-25) in his explanation of the Swiss Jurassic ironsto- Zone. This age is in accordance with Ji k Ziegler (1993) nes. It is possible that the beginning of the Ear|y nian- who aiso give the age of Polygnathus semrcostatus as gwlaris Zone might be represented in sample 13 in this from within Middle crepida Zone into the Late expansa environment obviously hostile to conodonts. Zone. At 292 m above the base of the section in the lower part of the "Cephalopod beds", P acutatus occurs 7. Latest marginifera Zone. with An. sinelarninws. According to Khalymbadzha et al. (1992, p. 75) the age the faunas from southern Kazak- At Kale Sardar in sample '!., 4.5 m above the base hstan associated with P. actuatus, including An. sinelarni- of the Niaz section, the conodont fauna included a zo- nus àîd iouaensis, "may perhaps correspond the nal species, Scaphignathws aelifer, as Sc. ee- I. to "Lelrfer v/ell as t78 M. Yazdi

ltfer leptus, Pelekysgnathus sp., Mehlina sp., Polygnatbus rnwnis collinsoni, and P semicostatus. The associated ce- communis comrnunis, P. semicostatws, P nodocostatus, Pal- phalopod fauna identified by Prof. Michael House (pers. matolepts glabra pectinata, Pal. margintfera marginifera, comm. 1995) includes: Cynoclymenia cf. inflata (Mun- Pal. mtnuta minwta, PaL schindeuolfi, and Pal. perlobata ster), and Platyclymenìa richteri Vedeking Group, the sigmoida, Although it is recognised that Pal. g. pectinau latter being typical of Famennian IV. Precise dating of is normally restricted to horizons no younger than Late the conodont fauna from this horizon wouid align this marginifera Zone, Ji k Zregler (1993, p" 15) record it as with Early expansa Zone. occurring in the Latest marginifera Zone. Sample 1 at Note: The Flowz-e-Dorah section appears to have Kale Sardar also has a diverse fauna of Famennian ce- a considerable hiatus at this level with the following zo- phaiopods including numerous species of Platyclymenia. nes not represented with certainty: Middle and Late ex- No samples have been processed from between pansa zoîes, Early, Middle and Late praesulcatA zoftes, 335 m and 339 m above the base of the section at sulcata Zone, Lower and Upper duplicata zones and Flowz-e-Dorah, an interval that might be of the same sandbergi Zone. Such a hiatus can be observed worldwi- age. As no platyclymeniids have been collected from the de due to a global regression. Compare, for example, the section at FIowz-e-Dorah, there is the possibility of the- history of the Michigan Basin documented by re being a hiatus for this time interval at Flowz-e-Dorah. Gutschick Ec Sandberg (1991) where a hiatus occurs from within th.e praesulcata Zone to the beginning of tlte crenulata Zone. B. Early expansa Zone. The incoming of. I. costatus darbyensis in sample 9. Early crenulata Zone. 16, 339 m above the base of the Howz-e-Dorah section is indicative of the Early expansa Zone. The presence of The first appearance of Si. isosticha is in sample faunal elements such as P perplexazs is consistent with 104, 384 m above the base of the Howz-e-Dorah section this age. Approximately 1 m above sample L6, crushed occurring in the bed lying unconformably immediateìy and scattered pieces of orthoceratids were collected. Ac- above the topmost unit of the "Cephalopod beds". This cording to Flouse (i981, p. 30), all ammonoids with the species first appears in the upper part of the crenuLata exception of the Prionoceratidae and Bactritina became Zone. The dominant conodont occurring with Sl. lsosli extinct at the end of the Late Devonian, approximately cha rs the long-ranging PoLygnathus inornatws. 95olo of the entire group disappeared. Vhere previously in the FTowz-e-Dorah section some beds consisted almost 1 0. isosticha-Upper crenu lata Zone. entirely of orthoceratids, the number of these fossils after Sample 521, 377 m above the base of the FIowz-e- sample 16 were reduced so far as to constitute less than Dorah section, yielded a specimen of Pseudopolygnatbus 5% in beds close to the top of Famennian. muhistriatus that, according to Lane et al. (1.980) occurs At 343 m above the base of the section in sample in beds no older than isosticha-Late crenulata Zone. 17, P. expetplexus and Clydagnatbus ormistont appear, two forms also consistent with an Early expansa age. 11. typicus Zone (: communis carina Zone). At Kale Sardar, in section A, sample 6 yieided a vast fauna of diverse cephalopods including numerous Fa- This zone is represented with certainty in the mennian orthoceratids. The Early expansa conodont Flowz-e-Dorah section with the occurrence of Dollymae fauna includes Bispathodus sabilis, Pseudopolygnatbus bouckaerti in sample 523, 180 m above the base of the controverslts, Polygnathus commwnis commwnis, P com- secrion (Conil et aI., 1,991; Sweet, 1988). Other elements

PLATE 1

Fig. 14, 15 x/0; figs 1-9,1.7,72,16 x100; fig. 10 x150; fig. 13 x2OO.

Fig. 1-4 - Icriodus iruaensis iouaensis Youngquist 6c Peterson, 1947: 1) upper view, EUIC 1821; 103 Howz-e-Dorah; 2) upper view, ELIIC 1822;103 F{owz-e-Dorah: 3) upperview, EUIC 1823; 103 llowz-e-Dorah; 4) lowerview, EUIC i823; 103 Flowz-e-Dorah. Fig.5 - Icriodus iouaensis iouaensis Youngquist & Peterson, 1947: narrow form, lateral view, EUIC 1824;51'1 F{owz-e-Dorah- Fig. 6-9 - Icriodus iouaensis imaensis Youngquist & Peterson, 1947: 6) upper view, EUIC 1825; 103 Howz-e-Dorah; Z) upper view, EUIC 1826;103 F{owz-e-Dorah: 8) upperview, EUIC 1827:IA3 Howz-e-Dorah; 9) upperview, EUIC i828; 103 Howz-e-Doreh Fig. 10 - Icriodus cf. L iotaaensis irntaensis Youngquist & Peterson, 1947: upper view, EUiC 1829 102 Howz-e-Dorah. Fig. 1.1,!3,l4Jcriodus alternatus Morphotype II Dreesen Ec Houlleberghs, 1980: 11) upper view, EUIC 18301 10J Howz-e-Dorah; 13) upper view, EUIC 1832; 102 Howz-e-Dorah; 14) upper view, EUIC 1833; 103 Howz-e-Dorah. Fig. 12 - Icriodus cf. L sp. aÍÍ. I. cornutus Sanneman, Clausen, Korn & Luppold, 1991: upper view, EUIC 1831; 103 llowz-e-Dorah. Fig. 15 - Icriodus al,ternatus tnd.@sonde n. subsp.: upper view, EUIC 1834; 103 Howz-e-Dorah. Fig. 16 - Icriodws afÍ. I. icruaensis Youngquist Ec Peterson, 7947:Kt element lateral view, EUIC 1835; 512 Howz--e-Dorah. Pl. 1 D ev on i an - Car b on i.fero u s C on o don ts /r om I r an 180 M. Yazdi

associated with this species are Polygnatbus communr currence of Gn. psewdosemiglaber are close to the end of commwnis, Idioprioniodws sp. and Gnathodus delicatus. the anchoralis-latus Zone, in other words, samples 14 Sample 9, a clast from the Sardar conglomerate at and 15 in section B at Kale Sardar are very ciose to the Kale Sardar, yielded Ps. pinndtus, P longiposticus, Gn. Tournaisian-Visean boundary. pseudosemiglaber and Gn. rypicws indicating a fauna o{ In the FIowz-e-Dorah section, ancboralis'latus typlcus age. Zone cannot be defined with precision but as the section is continuous and there is no sign of any hiatus 12. anchoralis-latus Zone. between the beds identified as belonging to the typícus Zone belovz and the texanils Zone above, further sam- The uppermost part of the ancboralis-latus Zone pling between these should yield diagnostic forms of an' can be recognised in sample 14, 38 m above the base of section B at Kale Sardar by the co-occurrence of choralis-latus age. Gnatbodws pseudosemiglaber, Gn. typicus and Gn. semi' Note: From the anchoralis-latus Zone to Carbonife- glaber.In sampie 15, 10 m above sample 14 in the same rous-Permian boundary, conodont zonatíon is problema- section, Sc. ancboralis europensìs occurs inter alia with tic as discussed in detail in Brenckle & Manger [eds] \Webster Gn. pseudosemiglaber and Cn. typicus and P symmetricus' (1991), for example in & Groessens (1991). Indi- Based on ranges given in Belka & Groessens (1986), the cative of the inherent problems, for the period above the last occurrence Sc. ancboralis europensis and the first oc- texnnus Tone and below the naaicwlus Zone, Sweet (1988)

PLATE 2

Figs 3, 4, 9 x60; fig. 10, 17 x8O; Íig. 1,2,8, 1'1, 12,15, 18-20, x100; fig. 5-7, 13' 74 x200; fig. 16 x250'

Fig. 1 - Icriodus sp. B.: 1) upper view, EUIC 1836; 504 Howz-e-Dorah; 2) lower view, EUIC 1836; 504 Howz-e-Dorah. Fig. 3, 4 - Icriodus alternatus mdwsonae n. subsp. 3) upper view, EUIC 1837;1,03 Howz-e-Dorah; 4) upper view, EUiC 1838; 103 Howz-e-Dorah. Fìg.5-10 - Icriodus aLternatus aLternatus Branson & Mehl, 1934a:5) upper view, EUIC 1839; 504 Howz-e-Dorah; 6) upper view, EUIC 1840;7 Niaz Section, Kale Sardar; 7) upper view, EUIC 1841; 11 Niaz Section, Kale Sardar; 8) upper view, EUIC 1842:103 Howz-e-Do- rah; 9) upper view, EUIC 1843; 103 F{owz-e-Dorah; 10) upper view, EUIC 7844;71 Niaz Section, Kale Sardar. Fig. 17,12 - Icriodus expanss.s Branson & Mehl, 1938: 11) upper view, EUIC 1845; 7 Kale Sardar; 12) upper view, EUIC 1856; 7 Kale Sardar. Fig. 13 - Ioiodus sp. A: upper view, EUIC 1847; ll Niaz Section, Kale Sardar Fig. 14 - Icriodus cornutus Sannemann, 1955: upper view, EUIC 1848; 518 Howz-e-Dorah' Fig. i5 - Icriodus costatus darbyensis Klapper, 1958: upper view, EUIC 1849; 16 F{owz-e-Dorah. Fig. 16, 17 - PeLekysgnatbus incLinatus Thomas, 1949: t6) lateral view, EUIC 1850; 1 Niaz Section, Kale Sardar; 17) laterù vìew, EUiC 1851; 1 Niaz Section. Kale Sardar. Fig. 18, i9 - Idioprioniodu.s spp.: 18) lateral view, EUIC 1852; 1OZ Howz-e-Dorah; 19) lateral view, EUIC 1853; 107 Howz-e-Dorah. Fig. 20 - cf . Idioprioniod.us sp.:lateral view, EUIC 1854;524 Howz-e-Dorah.

PLATE 3

Fig. 14, 15 x6O; fig. 2, 3, x80; fig. 1, 4-8, 12, 1.6 x\AO; [rg.9, ll, x12a;{iry. 10 x200; fig. 13 x550.

Fig. 1, 2 - Idioprionìodu.s spp.: 1) lateral view, EUIC 1855; 107 Howz-e-Dorah; 2) lateral view, EUIC 1856: I07 Howz-e-Dorah. Fig.3-8 - cf. Idioprioniodus sp.:3) lateral view, EUIC 1857; 533 Howz-e-Dorah;4) lateral view, EUIC 1858; 15 Niaz Section, Kale Sardar; 5) lateral view, EUIC 1859; 1OZ Howz-e-Dorah; 6) lateral view, EUIC 1860 707 Howz-e-Dorah; 7) la'teral view, EUIC 1861; 528 Howz-e-Dorah; 8) lateral view, EUIC 1,862:107 Howz-e-Dorah. Fig.9-13 - Locbriea com/nu.tdta (Branson & Mehl, 19a\:9) upper view, EUIC 1863; 108 Howz-e-Dorah; 10) upper view, EUIC 1864; 108 Howz-e-Dorah; 11) upper view, EUIC 1865; 108 Howz-e-Dorah; 12) upper view, EUIC 1866; 108 l{owz-e-Dorah; 13) enlargment of mìcrostructure on the central blade of EUIC 1865; 108 Flowz-e-Dorah. Fig. 14-15 -DollymaeboubaertiGroessens, 1971:14)upperview,EUIC1867;523Howz-e-Dorah;15) lowerview,EUIC186T 523F{owz-e-Dorah. Fig. 16 - NeogondolelLa cÍ. cLarki (K.oike, 1962) upper view, EUIC 1868; 109 Howz-e-Dorah.

PLATE 4

Fig. 1, 2, 4, 5,9, 72-14, x60; fig. 3, 6-8, 10, 11 x80; fig. 15 x100.

Fig.1-5 - Scaliognatbus ancboralis europensis Lane & Ziegler, !983:1) upper view, EUIC 1869;15 Niaz Section, Kale Sardar;2) iower view, EUIC 1869; 15 Niaz Section, Kale Sardar;3) upper view, EUIC 1870; 15 Niaz Section, Kale Sardar; 4) upper view, EUIC 1877;15 Niaz Section, Kale Sardar; 5) lower view, EUIC 1877;15 Niaz Section, Kale Sardar. Fig.6-11 -AncyrodeLLanodosarJlrich8cBassler, 1926:6)lower view,EUIC 1872:504 Howz-e-Dorah; 7) upperview,EUIC 1872;5A4 Howz-e -Dorah; 8) upper view, EUIC 1873; Ghale Kalagho; 9) upper view, EUIC 1874; Ghale Kalagho; 10) upper vieq EUIC 1875; 102 F{owz-e-Dorah; 11) lower view, EUIC 1'875; lQ2 Howz-e-Dorah. Fig. L2-I5 - Ancyrodella cureata (Branson & Mehl, 1934a): L2) lower view, EUIC 1876; 102 Howz-e-Dorah; 13) upper view, EUIC 1876; 142 Howz-e-Dorah; 14) upper view, EUIC 1877;7 Nraz Section, Kale Sardrr; i5) lrteral view of Sb elertent, EUIC 1878; 102 Howz-e- Dorah. Pl. 2 D eo a nìan- Car bon ifer o us C on o d on ts fr om Ir an LB1 182 M. Yazdi Pl. i Pl. 4 D e t on ian- C ar b on ifero us C on o do nts fro m I ran 183 1,84 M. Yazdi

labels the interval as one of "no widely recognised Zo- they show as the Tàpbrognatbodus transatlanticus Zone. nes". Zones given in Conil er al. (199\) are used herein. The occurrence of Gn. girtyi girtyi, in sample 28,609 m above the base of the Howz-e-Dorah section, indicates a 13a. "Early" bilineatus Zone (Visean). bilineatus age. Also occurring in this sample is Gn. semi- According to the zonation of Groessens (in Conil glaber, a species that, according to Zíegler (in Ztegler et dl., 1991, Fig. 2), there appears to be a dearth of cono- [ed.], 1981, p. 1,a7) may overlap with the occurrence of donts betwee n the texanus Zone and the bilineatws Zone Gn, bilineatus, the zonal form for this zone.

PLATE 5

Fig. 15, 16 x3O; fig. 13, 14 x40; fig.3-6,9'12, x60; fig. Z, 8 x80; fig. 1, 2 x100.

Fig. l-2 - Pseudopolygnatbus controuersus Sandberg & Ziegler, 1,979: 1) lower tiew, EUIC 1879; 6 Niaz Section, Kale Sardar; 2) upper view, ELJIC 1879;6 Niaz Section, Kale Sardar. Fig.3-12 - PseudopoLygnathus mubistriatzs Mehl & Thomas, 1947:3) upper view, EUIC 1880; 524 Howz-e-Dorah; 4) lower view, EUIC 1880; 524Howz-e-Dorah;5) lowerview, EUIC 1881;529 Howz-e-Dorah;6) upperview, EUIC 1881;529 Howz-e-Dorah; Z) uppervrew, EUIC i882; 524 Howz-e-Dorah; 8) lower view, EUiC 1882;524 Howz-e-Dorah; 9) lower view, EUIC 1883; 20 Howz-e-Dorah; 10) upper view, EUIC 1883; 20 Howz:e-Dorah; 11) upper view, EUIC 1884;524 Howz-e-Dorah; 12) lower view, EUIC 1'884;524 l{owz-e-dorah. Fig. 13-16 - Pseudopolygnatbus pinnatus Voges, 1959: 13) lower view of Morphotype I, EUIC 1885; 9 Niaz Section, Kale Sardar; 14) upper vrew of Morphotype I, EUIC 1885; 9 Niaz Section, Kale Sardar; 15) upper view of Morphotype II, EUIC 1886; 21 Howz-e-Dorah; 16) lower view of Morphotype II, EUIC 1886; 21 F{owz-e-Dorah.

PLATE 6

Fig. 14, 15 x4O; fig. 1, 3, 4, x6O; Íig. 2, 18-22 x80; fig. 5-13, 16, 17, 23 xlQ)'

Fig. 1 - Pseudopolygnathus pinnatus Voges, 1965: upper vreq EUIC 1887; 15 Niaz Section, Kale Sardar. Fig.2 - Pseudopolygnathus cf. triangulus inaequalis Voges, 1959: upper view, EUIC 1888; 15 Niaz Section, Kale Sardar^ Fig. 3-4 - Ancyrognatbus sinelaminus (Branson 8c Meh1, 1934a): 3) upper view, EUIC 1889; 511 Howz-e-Dorrh; 4) upper vieq EUIC 1890; 511 Howz-e-Dorah. Fig. 5 - Scaphignathus velifer leptusZieg\er & Sandberg, 1984: upper vieq EUIC 1891; 1 Niaz Section, Kjle Sardar. Fig.6-7 - Scaphignatbus oeliferLeLtfer Helms, 1959: 6) upper view, EUIC 1892; 1 Niaz Section, Kale Sardarr 7) upper view, EUIC 1893; 1 Niaz Section, Kale Sardar. Fig. 8-11 - Rhachistognatbus muricatus (Dunn, 1965); 8) upper view, EUIC 1894; 108 Howz-e-Dorah; 9) lower view, EUIC 1894; 108 Howz-e- Dorah; i0) upper view, EUIC 1895; 108 Howz-e-Dorah; 11) lower view, EUIC 1895; 108 Flowz-e-Dorah. Fig.L2-L3 - Polygnatbus aspelundi Savage 6c Funai, 1980: 12) upper view, EUIC 1896;503 Howz-e-Dorah; 13) lower view, EUIC 1896;503 Howz-e-Dorrh. Fig. 14-15 - Polygnatbus breoicarina Klapper & Lane, 1985: 14) upper view, EUIC 1897; 510 Howz-e-Doreh; 15) lower view, EUIC l89Zl 510 -Flowz-e-Dorah. Fig"76,23 - Polygnatbus aequalis Klapper & Lane, 1985: 16) upper view, EUIC 1898; 102 Howz-e-Dorah;23) upper vìew, EUIC 1994;507 f10wz-e-ìJoran. Fig. 17 - Polygnathus cf. dcutatus Khalymbadzha, Shinkarov & Gatovsky, 1992: upper view, EUIC 1899; 511 Howz-e-Dorah. Fig. 18-19 - Bispathodus stabilis (Branson & Mehl, 1934a): 18) lower view, EUIC 19OO; 6 Niaz Section, Kale Sardar; 19) upper view, EUIC 1900; 6 Niaz Section, Kale Sardar. Fig. 20 - Spatbognatbodz.d sp.; upper view, EUIC 1901;525 Howz-e-Dorah. Frg.2l-22 - Mehlina spp.:21) lateral view, EUIC 1902; 77 Howz-e-Dorah;22)lxeral view, EUIC 79A3;1'6 Howz-e-Dorah.

PLATE 7

Fig. 1-5, \1, 1,2, 77-20 x60; fig. 7 x7A; fig. 6, 16,21,22 xlAAi fig. 9' 10, 14, 15 x720; fig. 8' 13 x150.

Figs 1-2 - Polygnathus tff. P angustidi.sczrs Youngquist, 1945: 1) upper view, EUIC 1905; 509 Howz-e-Dorah; 2) upper view, EUIC 1906; 509 l-lowz-e-lJoran Figs3-6 - Polygnatbus erid.ens Klapper 6c Lane, 1985: 3) upper view, EUIC 1907; 510 Howz-e-Dorah; 4) upper view, EUIC 1908; 7 Niaz Section, Kale Sardar;5) lower view, EUIC 1909;7 Niaz Section, Kale Sardar; 6) upper view, EUIC 19fi;1'02 Howz-e-Dorah. Ftg.7-13,1,5- Polygnathus communis communis Branson 6c Mehl, 7934a:7) upper view, EUIC 1911; 104 Howz-e-Dorah; 8) upper view, EUIC L912; 523 Howz-e-Dorah; 9) lower view, EUIC 1972;523 Flowz-e-Dorah; 10) upper view, EUIC l9I3;524 Howz-e-Dorah; 11) lower view, EUIC 1913; 525 Howz-e-Dorah;12) upper view,.EUIC 1914; 16 Howz-e-Dorah; 13) upper view, EUIC 1915; 104 Howz-e-Dorah; 15) lower view, EUIC 1977;20 Howz-e-Dorah. Fig. 14, 16 - Polygnatbus cf. P communis collinsoni Druce, 1966: 14) upper view, EUIC 1916; 6 Niaz Section, Kale Sardar; 16) upper view, EUIC 1918; 6 Niaz Section, Kale Sardar. Fig.17-20 - Polygnathws planarius Klapper & Lane, 1985; 17) upper view, EUIC 1919; Ghale Kalagho, F{owz-e-Dorah; 18) upper view, EUIC 1920; Ghale Kalagho, F{owz-e-Dorah; 1.9) upper view, EUIC 1921; Ghale Kalagho, Howz-e-Dorah; 20) lower view, EUIC 1921; Ghale Kalagho, FIowz-e-Dorah. Fig.21,-22 - PoLygnatbws cf . experplexus Sandberg & Zìegler, 1979: 21) upper view, EUIC 1922; 77 Howz-e'Dorah; 22) lower vrew, EUIC 19221 17 Howz-e-Dorah. Detonian-Carboniferous Conodonts from lran 185 i86 M. Yazdi Pl.7 De't,onian-Carboniferous Conodonts from [ran 187 188 M. Yazdi

13b. "Late" bilineatus Zone (Namurian). (Lane & Straka, 97a). The naaiculus Zone of Sweet This informal subdivision of the bi/ineatus Zone (1988) would, therefore, be the equivalent o{ the bilinea- equates with the base of the girtyi simplex Zone {irst tus Zone (Namurian) used herein and to the lower part recognised by 'Webster (1,969) in sequences in south- of the girtyi sirnplex Zone as the occurrence of Gn. gir- western Nevada and iater applied to sections in England tyi simplex is given by Higgrns (1985) as from the base (Higgins, 1975, 1985). From sections in Arkansas and of the Namurian. Its occurrence with Gn" girtyi inter- Oklahoma, the interval recognised by Webster (1969) on medius in sample 29, 646 m above the base of rhe the grounds that the girtyi sirnplex Zone is represented FIowz-e-Dorah section indicates the upper part of the by the Caawsgnathus naoiculus and C. unicornis zones bilineatus Zone or Late bilineatus Zone as used herein.

PLATE 8

Ftg.2,7, 1.2-1.4 x60; tig. l,3-6,8, 11, 15-20 x100; fig. 9, 10 x120.

Fig. i-5 - Polygnathus inornatus E. R Branson, 1934: 1) upper vieq EUIC 1923; 104 Howz-e-Dorah; 2) upper view, EUIC 1.974;51.8 Howz-e- Dorah; 3) lower view, EUIC 1925; 104 Howz-e-Dorah; 4) upper view, EUIC 1926;104 Howz-e-Dorah; 5) lower vrew,EIJIC 7927; 104 Howz-e-Dorah. Fig. 6, 17 - Poiygnatbus perpLexus Thomas, 7949: 6) upper view, EUIC 1928; 16 Howz-e-Dorah; i7) upper view, EUIC 1938; 16 Howz-e-Dorah. Fig. Z - Polygnathus cf. papilata Youngquist 6c Peterson, 1947: tpper view, EUIC t929; 14 llowz-e-Dorah. Fig.8-11 - Polygnatbus sem;costdtus Branson & Mehl, L934a:8) upper view, EUIC 1930; 516 Howz-e-Dorah; 9) upper view, EUIC 1931:516 Howz-e-Dorah; 10) upper view, EUIC 7932;6Nraz Section, Kale Sardar; 1l) upper vrew, EUIC 1q33; 516 llowz-e-Dorah. Fig. 12 - Polygnatbus cf. unicornis Miiller 6a Mùller, 1957: upper view, EUIC 1934; 510 Howz-e-Dorah. Fig. 13, 14 - Polygnathus sp. A: 13:upper view, EUIC i935; 11 Niaz Section, Kale Sardar; 14) upper view, EUIC 1936; ).03 Howz-e-Dorah. Fig. 15, 16 - Polygnathus sp. B: 15) upper view, EUIC 1937;16 Howz-e-Dorah; 16) lower view, EUIC 1937; 16 Howz-e-Dorah. Fig. 18 - Polygnatbus longiposticus Branson & Mehl, 1934a: upper view, EUIC 1939; 9 Nìaz Section, Kale Sardar. Frg. L9"20 - Polygnathws cf . symmenicus Branson, 1.934 19) upper view, EUiC 1940; 15 Niaz Section, Kale Sardar; 20) lower view, EUIC 1940; 15 Niaz Section, Kale Sardar.

PLATE 9

Fig. to x5Or lig. l,-5, x6O: figs l.2,6-15, I7,2l xlOOr fig. 20 xl2Or lig. l9 x150, fig. l8 x2OO

Fig. 1-5 - Polygnathus ratebi n. sp.: 1) upper view of paratype, EUIC 1941; 103 Howz-e-Dorah; 2) lower view of paratype, EUIC 1941; 103 Howz-e-Dorah; 3) upper view of holotyp, EUIC 1.942; i03 Howz-e-Dorah; 4) lower view of holotype, EIJIC 1942: 103 Howz-e- Dorah; 5) upper view of paratype, EUIC 1943; 103 Howz-e-Dorah. Fig.6-72 - Polygnathus capollocki n. sp.: 6) upper view of paratype, EUIC 7944; 102 Howz-e-Dorah; 7) upper view of paratype, EUIC 1945; 102 Howz--e-Dorah; 8) upper view of holotype, EUIC 1946; 102 Howz-e-Dorah; 9) lower view of holotype, ErJIC 1946: 1.02 Howz-e-Dorah; 1O) lateral view of paratype, EUIC L947;102 Howz-e-Dorah; 11) lateral view of pararype, EUIC 1948; lA2lrJlwz- e-Dorah; 12) upper view of paratype, EUIC 1949; 102 Howz-e-Dorah. Fig. 13-15 -PolygnatbusuebbiSr.aufÍer, 1938:3) upperview,EUIClg50;102Howz-e-Dorah;14) lowerview,EUIC19SA;fi2 llowz-e-Dorah; 15) upper view, EUIC 1951; 3 Niaz section, Kale Sardar. Fig. 16 - Polylophodonta confluens (Ulrich 6c Bassler, i926): upper view, EUIC 1952; 516 Howz-e-Dorah. Fig. 12, 18 - Palmatolepi mìnuta minuta Branson & Mehl, 1934t 17) upper view, EUIC 1953; 11 Niaz Section, Kale Sardar; 18) upper view, EUIC 1954; 103 Howz-e-Dorah. Fig. 19 - Palmatolepis marginifera marginifera Helms, 1959: upper vrew, EUIC 1955; 1 Niaz Section, Kaie Sardar.

Fig.2A,21 - Palrnatolepis glabra pectinata Zregler, 1962:20) upper view, EUIC 1956; 1 Niaz Section, Kale Sardar; 21) upper view, EUIC 195/; 1 Niaz Section, Kale Sardar.

PLATE 10

Fig. 16, 17 , 18 x5O; fig. 6,7 , 10-12, 14, x60; fig. 5, i3, 15, x80; fig. 1-4, 8, 9, x1OO.

Fig. 1-3 - PaLntatolepis minuta tninuta Branson & Mehl, 1934a: 1) upper view, EUIC 1958; 1 Niaz Section, Kaie Sardar; 2) upper view, EUIC 1959; 1 Niaz Section, Kale Sardar; 3) upper view, EUIC 1960; 1 Niaz Section, Kale Sardar. Fig.4 - Palmatolepis schind.etaoffi Mùller, 1956: upper view, EUIC 1961; l Niaz Section, Kale Serdar. Fig. 5 - PalmatoLepìs perlobata sigmoida. Zieg\er,7962: upper view, EUIC 1962;1 Niaz Section, Kale Sardar. Fig.6,7,I4 - Palmatolepis subperlobata Branson & Mehl, 1934a: 6) upper view, EUIC 1963; 103 Howz-e-Dorah; 7) lower view, EUIC 13ú; 1A3 Howz-e-Dorah; 14) upper view, EUIC 1969; fi3 Howz-e-Dorah. Fig8,9 - PalntatoÌepts quadrantinodosalohata Sannemann, I955: 8) upper vrew, EUIC I964t ll Nrrz Section, Kale Sardrr: 9) upper view. EUIC 1965; 11 Nìaz Section, Kale Sardar. Fig. 10-12 - Palmatolepis tenuipunctatd Sannemann, 1955: 10) upper view, EUIC 1966; 103 Howz-e-Dorah; 11) lower view, EUIC 1966; 1Ol Howz-e-Dorah; 12) upper view, EUIC 1867; 103 Howz-e-Dorah. Fig. 13 - Palmatolepis cÍ. tenuipunctata Sannemann, 1955: upper view, EUIC 1968; 103 Howz-e-Dorah. Fig. 15 - Palmatoiepis sp. A: upper vieq EUIC 1970; 3 Niaz Section, Kale Sardar. Fig. 1.6, 17 - Palmatolepis sp. C: 16) upper view, EUIC 1971;16 Howz-e-Dorah; 17) lower view, EUIC 1971; 16 Howz-e-Dorah. Fig. 18 - Palmatolepis sp. B: upper view, EUIC 7972;7 Niaz Section, Kale Sardar. D e rt on ian - C ar bonifer o u s C on o don ts fr o m Ir an 189 190 M, Yazdt PÌ, 9 Pl. 10 - D eo o nian Car b on ifero u s C on o donts from Ir an 191 t92 M. Yazdi

Note: The bollandensis Zone ís not clearly repre- 1 4. slnuatus- co r ru g atu s - s u I c atu s Zone or you n g er. sented in the Flowz-e-Dorah section. Although 7 pro- The presence of Declinognatbodus noduliferus, ductive horizons were processed in the 71'4 m between Idiognathoides sinuatus and Rhachistognathus muricatus horizons of Late bilineatus age to those of nodwliferus in the base of the crinoidal limestone in sample 108, Zone, no diagnostic conodonts oÍ bollandensis age were 820 m above the base of the section at Flowz-e-Dorah recovered. are indicative of an age no older than fhe sinuatus-corru-

PLATE 11

Fig. 3, 9 x6O; fig. 1 x75; fig.4-8, 10-15, 19, 20 x100; fig' 2, t6' i7, 18 x160.

Fig. 1 - PalmatoLepis uincheLli (Stauffer, 1938): upper view, EUIC 1973;7 Níaz Section, Kale Sardar. Fig.2 - Palmatolepìs sp. D: upper view, EUIC 7974;2Ni:rz Section, Kale Sardar. Fìg. 3, 4 - PaLmatolepis tuolskae Ovnaranova, 1969: 3) lateral view of Pb element, EUIC 1975; 1 Niaz Section, Kale Sardar; 4) lateral view of Pb elernent, EIIIC 7976;1 Niaz Section, Kale Sardar. Fig. 5, 6 - ALtemognathus c[. regularis Zìegler & Sandberg, 1984: 5) lower view, F,TJIC 1977; 4 Niaz Section, Kale Sardar; 6) upper view, ELJIC 7977:4 Niaz Section, Kale Sardar. Fig. 7, 8 - Siphonodella isosticha (Cooper, 1939):7) upper view, EUIC 1978; 104 Howz-e-Dorah; 8) upper view, EUIC 7979; 1A4 FIowz-e-Dorah. Fig.9 - SipbonodelLa cf. obsoleta Hass, 1959: upper view, EUIC 1980; 104 Howz-e-Dorah. Fig. 10-19 - Gnathodus pseudosemiglabez Thomson & Fellows, 1970: 10) upper view, EUIC 1981; 107 Howz-e-Dorah; 11) upper vìew, EUIC 1.982;75 Niaz Section, Kale Sardar; 12) upper view, EUIC 79$; lA7 Howz-e-Dorah; 13) upper view, EUIC i984; 15 Niaz Section, Kale Sardar; 14) lower view, EUIC 1983: 1Q7 Howz-e-Dorah; 15) upper view, EUIC 1985; 13 Niaz Section, Kale Sardar; 16) upper view, EUIC 198ó; 13 Niaz Section, Kale Sardar; 17) upper view of transtional form between Gn. pseudosemiglaber and Gn, girtyt, EUiC 1987; 108 Howz-e-Dorah; 18) upper view of transtional form between Gn. pseudosemiglaber :.nd Gn. girtyi, EUIC 1988; 108 Howz-e-Dorah; 19) upper view of transtional form bet'ween Gn. pseudosemiglaber a,nd Gn. girtyi, EUIC 1989; 108 Howz-e-Dorah. Fig. 20 - Gnatbodus bilineatus (Roundn 1926): upper view, EUIC D9a; B Niaz Section, Kale Sardar.

PLATE 12 Frg.8x6O;fig.21,,22x85;fig.5x95;fig.1-4,5-7,9,13,x100;fig.18x110;{ig.14,15x120;fig.1.1,12,19,2A,23x130;fig.10x140;frg.16,\7x1s0.

Fig. 1-3, 5 - Gnathodus girtyi intermedlzs Globensky, 1967: l) upper view, EUiC 1991; 36 Howz-e-Dorah; 2) upper view, EUIC 1992; 29 Howz-e-Dorah; 3) upper view, EUIC 1993:532 Howz-e-Dorah; 5) upper view, EUiC 1995;29 Howz-e-Dorah. Fìg. 4 - Gnathoclus pseudosemigLaber Thompson Ec Fellows, 1970: rpper view of transitional form between Gn. pseudosemigLaber and Gn girtyi, EIJIC 1994; 9 Niaz Section, Kale Sardar' Fig. 6-8 - Gnathod'us semigLaber Bischoff, 1957: 6) ìower view, EUIC 1996; 107 Howz-e-Dorah; 7) upper view. EUIC 1996: L07 Howz-e-Do rah; 8) upper view, EUIC 1997;74 Flowz-e-Dorah. Fig.9,I7,l2- Gnathorius girtyi girtyi Hass, 1953: 9) upper view of early form, EUIC 1998; 108 Howz-e-Dorah; 11) upper view, EUIC 2000; 108 Howz-e-Dorah; 12) upper view, EUIC 2001; 108 llowz-e-Dorah. Fig. 10 - Gnatbodus typicus Roundy, 1926: tpper view, EUIC 1999; 13 Niaz section, Kale Sardar- Fig. 13-18 - Gnathodus girtyi simpLex Dunn, 1965: 13) upper view, EUIC 2A02;7A7 Flowz-e-Dorah; 14) upper view, EUIC 2003; 108 FIowz-e- Dorah; 15) lower view, EUIC 2003; 108 Howz-e-Dorah; 16) upper view, EUIC 2004; 108 llowz-e-Dorah; 17) lower view, EUIC 2OO4; 108 Howz-e-Dorah; 18) upper vierlu, EUIC 2005; 108 F{owz-e-Dorah. Fig. 19, 20 - Gnatbodus delicatus Branson & Mehl, 1938: 19) upper view, EUIC 2006; 523 Howz-e-Dorah; 20) lower view, EUiC 2006; 523 f10wz-e-lJoran. Fig.2I-23 - DecLinognathodus noduliferus noduliferus (Ellison 6ú Graves, L9a\: 21) upper view, EIJIC 2007; 108 Howz-e-Dorah; 22) lower view, EUIC 2O0Z; 108 Howz-e-Dorah; 23) lower view, EUIC 2008; 108 Howz-e-Dorah.

PLATE 13

Fig. 3, 11, 14 x6O; fig. 18 x65; {ig. 4 x7A;14 x8O; fig. 17 x85; fig. 7,5,7,8,10,72,76,19 x100; fry.2,6,9, x120; fig. 13, 15 x130.

Fig. 1-3 - DecLinognatbodus noduLiferus noduliferus (Ellison & Graves, 1941): 1) upper view, EUIC 2AO9; 73 Nìaz Section, Kale Sardar; 2) upper view, EUIC 2O1O;13 Niaz Section, Kale Sardar; 3) upper view, EUIC 2A71; L3 Niaz Section, Kale Sardar. Fìg. 4 - Neognatlsodus cf . medadultimu.s, Merrill, 1972: tpper view, EUIC 2A1,2; 108 F{owz-e-Dorah fig. S-l - Id.iognatboides sinuatus Flarris 6r Hollingswonh, 1933: 5) upper view of early form, EUIC 2013; 108 Howz-e-Dorah; 6) upper view, EUIC 2014; 9 Niaz Section, Kale Sardar; 7) upper view, EUIC 2015; 108 F{owz-e-Dorah" Fig. S - lGnatbodus sp.: upper view, EUIC 2016;13 Niaz Section, Kale Sardar' 2a18; 107 lIowz-e-Dorah. E;!. I, f O - Gnathodus sp: 9) upper view, EUIC 2Ot7; lO7 Howz-e-Dorah; 10) upper view, EUIC f;g. tt, tZ - CLydagnatbus lorntistonì Beinen, Klapper, Sandberg k Ziegler, 1971.: 11) lateral view, EUIC 2019; 17 Howz-e-Dorah; 12) upper vieq EUIC 2A22; 17 F{owz-e-Dorah. Fig. 13 - "Hindeodella" segaformis Bischoff, L957:Iatenl view, EUIC 2021;15 Ni.rz Section, Kale Srrder. f;i. t+-lZ - Unassigned 14) lateral vieq EUiC 2A22; 15 Niaz Section, Kale Sardar; 15) laterel view, EUIC 2023: 75 Niaz Section, "I"À.rtr' Kale Sardar; 16) lateral view, EUIC 2024; 15 Niaz Section, Kale Sardar; 17) lateral view, EUIC 2025: 15 Niaz Section, Kale Sardar. Fig. 1g - ?Pseudopolygn4tbus sp.: lateral view of Sb element, E\JIC 2026: 516 Howz-e-Dorah. Fig. 19 - Idiognathoides sp. lateral view of Sc element, E\JIC 2027:107 Howz-e-Dorah' D e a ontan- Car bon ifero u s C on o don ts fr om lr an 793 M. Yazdi Pl. 12 Pl. 13 D eoon ian- C ar bon ifero us C on odonts fr o m I r an t95 196 M. Yazdi

gat u s - s u I c at u s Zone. Altho ugh. Lo ch r ie a c o nx?rlu ta La, anof- 16. Late Namurian. her element in the fauna from sample 108, is generally A single specimen of Neogondolella clarki was re- thought to have its latest occurrence below this zone covered from sample IO9,97I m above the base of the (e.g. Conil et al., 1991), it has been reported ro occur in section ar FIowz-e-Dorah. According to Sweet (19gg) the sinuatus Zone in the Pyrenees (Perret & Weyant, Neogondolella first appears in the late Namurian (:Ato- 1994).In a clast from the Sardar conglomerate, sample kan). The bed yielding Neogondolella clarki conrains a 13, at Kale Sardar, Idiognathoides sinuatus was recovered highly diverse fauna of brachiopods. together with Declinognathodws noduliferus, Lochriea co?nmutata, and Gnathodus pseudosemiglaber indicating 17. Age of lhe Sardar conglomerate the ciast to be at least sinuatus-corrugdtus-sulcatus in age. Gn. bilineatus, normally thought not ro exrend beyond The age of the Sardar conglomerate is controver- the noduliferws Zone, is also present in the fauna; this is sial (e.g. Stócklin et al., 1965,1991; Husseini, 1992).In another form reported by Perret & Weyant (1994) to oc- order to have more precise age control over the time of cur in the sinuatus Zone in the Pyrenees. Biogeographi its deposition, 5 limestone clasrs from the Niaz section caily, the Pyrenees and Iran, both situated on the nofth- at Kale Sardar were processed for conodonts. Faunas ern margin of Gondwana, must have been in close jux- from the clasts are representarive of 4 different zones: taposition at this time thus explaining the similar ranges Late triangularis Zone or Early crepida Zone, typicus for both Lochriea comrnutata and Idiognatboides sinuatus. Zone, ancboralis-latus Zone and sinuatus-corrugatus-sulca- At least 5 goniatites identified as beyrichoceratids tus Zone. From this data alone, the Sardar conglomerate or reticuloceratids (Prof. M. Flouse, pers. comm. , 1993, must have been deposited some time after the sinwatus- 1995) were collected from sample 108 ar Howz-e-Dorah. corrugatus-sulcatus Zone. The cephalopods from sample 108 in the FIowz-e-Dorah section occur with a fauna of conodonts dated as sinwa- 'l L Permian. tus-corrugatus-sulcatus Zone, an age consistent with the Namurian age for the genus Reticuloceras. Beyrichocera- The siliclastics ("]ù7hite Quartzite") cropping out between tids, however, are known to occur in older horizons. 1008 m and 1038 m above the base of the sec- permian From easrern Australia, Campbell et al. (tlSt) reported tion at FIowz-e-Dorah represent basal (Asse- four species of Beyricboceras occ,,s,rríng in horizons that lian) (Partow Azar, 1992). Investigation of conodonts from iimestone can be aligned with the upper parr of the Visean (p. ZZ, this was outside the scope of this study Table 1 and78, fig. 2) and Roberts et al. (tllt) align the but macrofauna collected from sample L1O from 1055 m \West above European Beyrichoceras Zone with the .late Visean. the base of the section include numerous Permian Lemosquest et al. (1985) reported the disappearance of species of Fenestella, Bellerophon, other gastropods, bra- Carboniferous goniatites including Beyrichoceras in the chiopods, bivalves and crinoid remains. late part of Visean in North Africa. If further study of the goniatites prove the specimens from F{owz-e-Dorah Systematic palaeontology. to be beyrichoceratids, this will exrend rheir range rnto the Namurian. With the constraining age of the cono- Acid leaching 110 samples collected from two 1o- donts on this goniatite fauna, precise identification of the calities in the Shotori Range, Easrern Iran produced specimens will be useful for future correlatibns. 3445 conodonts representing 85 species/subspecies. Three of these are new and are described below. As re- 15. Upper part of the Namurian (= Westfalian). cent synonymies are have been published for the other species (..g. &. Ziegler, 1993; Mawson & Talent, No conodont data is available for the 138 m of Ji 1997), the faunas are documented (Plates 1-13, Tables 1- section above sample 108 at Flowz-e-Dorah. At 958 m 3) but no taxonomic commenr is given. All figured spe- above the base of the section in sample 500, specimens of cimens from the area are deposited at the University of Gastrioceras sp., a genus known to occur in the upper Esfahan, Iran, bearing the prefix EUiC. quarter of the Namurian (: .Westfalian), were collected (identified by Prof. M. FIouse, pers. comm. , 1993, 1995). Phylum Conodonta Gastrioceras sp., identified by O. \falliser, was also repor- Pander, 1.856 ted from Kale Sardar by Stócklin et al. (199I) from his Order Conodontophorida Eichenberg, 1930 horizon 35 in the type section of the Sardar Formation. Family I c r i o do nr i dae MùllerandMiiller, 1952 The presence Gastrioceras of sp. in the Late Car- Genus lcriodus Branson and Mehl, 1938 boniferous allows correlation of the Sardar Formation at Kale Sardar and FIowz-e-Dorah. Type species. Icriodus expansus Branson and Mehl, 1938 Devonian-Carboniferous Conodonts from lran 197

lcriodus alternatus mawsonae n. subsD. Holotype. EUIC1947, the specimen illustrated on PI.9, Figs. 8, 9 from sample 102, 205m above the base Pl. 1, Fig. 15; Pl. 2, Fig.3,4 of the Howz-e-Dorah section. Diagnosis. A species of Polygnathus with a 1ong, very narrow 1991 Icriodus alternatus n. subsp. Clausen, Korn and Luppold, pl. 8, rlg, r+. and siightly curved platform that has a shagreen surface excepr for nodes along the upturned margins; deep adcarinai trough developed almost the entire Derivalion of name. In honour of Prof. Ruth Mawson, an length of the platform. Austraiian conodont researcher.

Holotype. EUIC i834, the specimen illustrated on the Plate 1, Description. A species of Polygnathw.s with a slender, fis. I5 from s;mnle l0l 115 m above the base of the Howz-e-Dorah arrow-shaped platform; the posterior end is very poinred. "tttot Platform surface is shagreen lacking ornament excepr for o,unnosis. A subspec ies oÍ Icriodus alternatuswith a row of tiny and/ or fused nodes that may develop along the mar- verl' weakly expressed nodes located in a central trough between late- gins in the anterior half of the platform. The carina is ral rows of nodes. Basal cavity follows the shape of the spìnd1e, e$an- .li.-,.^"r",i^.t.. almost straight and does not reach the posterior end. The margins of the platform are sharply upturned forming Description. Between lateral rows of discrete nodes, two deep troughs on either side of the carina that run for a central row of poorly expressed nodes lies in a slight more than three-quarters the length of the platform. The trough. Towards the.anterior, orÌe or two of the iateral length of the free blade approaches that of the platform nodes may be fused. The basal cavity flares considerably and is made up of eight to ten clear, sharp denticles. posteriorly and tapers evenly towards the anterior; a Remarks. The specimens from Iran are similar to slight spur is developed along the outer margin. the specimens from Alberta, Canada, illustrated by Pol- Remarks. The specimen illustrated by Clausen er lock (1968, pl. 62, Figs. 32, 33, 38). The polygnathid al. (1.991, pl. 8, fig. 4), at first glance appears ro be an from the Timan Formation, Russian Platform illustrated aberrant form of I. a. alternatus with the central nodes by Kuz'min (1995, pl" 2, tig.7) appears m be a specimen poorly developed. However, as L5 specimens, all of P capollocki. The Iranian material came from samples showing this characteristic, have been recovered from yielding Ad. curaaa late form indicating that in Iran the sample L03, a new subspecies, as suggested by Clausen er age of this conodont can be said to be from late in the al. (1,991), appears warranted. The central trough be- F,arly hassi Zone to the end of the lingutformis Zone (Ji tween the lateral rows of denticles bears tiny central no- & Ziegler,1993). Its earlier appearance in Russia des, most clearly visible towards the middle of the ele- (Kuz'min, 1995) is indicative of an older age. ment. Anteriorly the nodes are fused. A second feature Occurrence. One Pa element from sample 503, two that identifies this as a separate subspecies is the basal from sample 9, three from sample 505, one from sample cavity; it is larger than that of I. alternatus sensu strrcto. 10, 34 from sample 1.02, one {rom sample 508, two from The sample yielding the new subspecies also contains sample 509, and one from sample 510 at Howz-e-Dorah" PaÍ" tenuipunctata, Pal. minuta ?ninuta, and I" iowaensis Three Pa eiements from sample 3 at Kale Sardar" iozuaensts suggesting the age to range from the Late triangularis Zone to the Eariy lepida Zone. L alternatus Polygnathus ratebi n. sp. ?na'.asonae occurs in horizons of similar age in a section (Pl. 9, Figs. 1-s) at Kuragh Spur, Chitral, Pakistan (Mawson, pers. comm,

1.997; Talent et al., 1999). Derivation of name. In honour of Farajoalah Ratebi, a Natio- Occurrence. Fifteen I elements from samole 103 at nal lranian Steel Company geologist, who spent most of his working Howz-e-Dorah. life in exploration of coal and raw marerials in Tabas and centrd lran. Holotype. EUlClg42, the specimen illustrated on Pl. 9, Figs. 3, 4 from sample 103, 312.50 rn above the base of the Howz-e-Dorah Family P o I y g n aî h i d a e Bassler, 1925 section" Genus Polygnathus Hinde, 1829 Diagnosis. A species of PoLygnatbus with shon crrrnr exten- ding to half the length of the platform with strongly upturned, almost Type species. Polygnathus dubius Hjnde, 1879 smooth platform margins forning deep adcarinal troughs. Linguloid posterior half of the platform ìs covered by complete or interruptecl ridges. Polygnathus capollocki n. sp. Pl. 9, Fig. 6-12 Description. A species of Polygnatbus with a c^rifla made up of fused denticles extends to the midlength of the 1968 Polygnathus n. sp. A. Pollock, p. 436, p1. 62, fig. 32,33,38. platform; the platform margins paralleling the carina are 1995 Polygnathus c[. xylus Stauffer, Kuz'min, pl. 2, fig.7 sharply upturned forming smooth, deep adcarinal

Derivation of name. In honour of C.A. Pollock who. in 1968. troughs. The platform is very narro.w at the anterior but recognised thrs form rs a new species. widens gradually reaching maximum width at midlength 198 M. Yazdi

of the platform. In the posterior half of the platform, carried out. I thank my supervisors, Prof. John A. Talent and Prof. Ruth Mawson their instruction, cornments supervrsron. paraliel ridges, some complete and some discontinuous, for and Thanks are extended to Prof. Michael House from the University of cover the tongue. The ridges on the platform are parallel Southampton and Prof. Rex E. Crick from the University of Texas at or semi-paraliel, sometimes becoming weakiy nodose Arlington, for their co-operation and identification of cephalopods. especially close to the carina. Prof. G. Klapper, Dr. R. T. Becker, Dr. Z. Belka and Dr. P J. Conaghan kindly commented on various aspects of the study. This Remarks. P. ratebi n. sp. shows some simiiarities to paper has benefitted trernendousLy from the comments and Polygnathus samueli Klapper & Lane (1985, p. 943, fi.g. suggestions made by Profs Ruth Mawson and Claudia Spalletta and 17.13-18) but the platform shape and the form of basal another unnamed assessor. Special thanks are due to the members of ny famrly: my cavity are different from P samweli as P ratebi has a tiny father who encouraged me dunng his life even on the day before he basal cavity, and a narrow platform with parallel uptur- passed awan my mother, sister and brothers especially my first ned anterior margins. In their consideration of the phy- brother, Moharnmad Yazdi and members of his office in Tehran. I logeny o{ the semicostatus group, Ji Et Ziegler (1993, p. am indebted to my wife Zahra Khademmelat who helped me during field work, with processing srmples rnd wirh polytungstate 43) suggest that there might be an intermediate form be- separations. My children, Meysam, Mohamrnad and Elham Yazdi tween P breaicarinus and P semicostalus (wide-platform worked hard at school in Australia learning English. I arn grateful to morphotype). Such a transitional form, they conclude, all members of my wife's famiiy who helped by sending books, might arise in the Early triangularis to the Early crepidd documents and fossils to Australia from Iran. I will never forget their encouragement. A1l effons made by family members, Khademmelat, association other cono- interval. As it is found in with Rozegrrirn and Mrlekrhr rre grertlr rpprecirted. donts that can be dated as from the Late triangularis Transponing samples frorn Tebas to Esfahan would have been Zone to the Late crepída Zone, and because of its mor- impossible without the co-operation of the Exploration Group of the Metal Supply Comprny Pyrbekran, Esfahan phologicai characteristics, P ratebi couid possibly be the Non Minerrl at (N.I.S^C) and the Geology Depanment of Esfahan University. I ancestor of P semicostatus" appreciate the encouragement given me by friends and colleagues at Occurrence. Eight Pa elements from sampie 103 at NISC, Esfahan University and the Geological Survey of Iran. FIowz-e-Dorah. Friends {rom the Macquarie University Centre for Ecostratigraphy and Palaeobiology were most generous with their assistance. I am especially grateful to: Michael Engelbretsen, George AcknozoLedgemmts. Vilson, Theresa \flinchester-Seeto, Glenn Brock, Margaret Anderson, I am deeply indebted to the government of the Islamic Ross Parkes, David Matheison, Paul Farquharson, Alison Basden, Republic of Iran and the Ministry of Culture and Higher Education Julie Trotter and other rnernbers of MUCEP. These, with my Iranian of lran. The Esfahan University supported me financially during the friends and colleagues at Macquarie, helped to make my research a period of my research in Australia where this investigrtion was friendlv and fruitful exoerience.

REFERENCES

Be|ka Z. & Groessens E. (1986) - Conodont succession across conodonts in the Franco-Belgian and Campine Basì.ns: the Tournaisian-Visean boundary beds at Salet, Bel- Their potential for widspread correlatior. Courier glii-m. Bull. Belg. Wrenig. Geol., v. 95, pp. 257-280, Brus- Forscb. Senckenb., v. 73A, pp. 15-10. Frankfurt-am-Main. sels. Dreesen, R. Ec Dusar, M. (1974) - Refinement of conodont Branson E.B. E( Mehl M"G. (1938) - The conodont genus biozonation in the Famenne-Type area. GeoLogical Swru. Icriodus and its stratigraphic distribution. fourn. Pa- Belgium PubL., v. 1,3, pp. 1,-36, Brussels. leont., v. 12, pp. 156-166, Tulsa, Oklahoma. Flùgel E. (1966) - Iranoblastus, a new Mississippian blastoid Brenckle P.L. & Manger \LL" {1991) - Intercoritinental corre- from Iran. In: Contributions to the Paieontology of latron and division of the Carboniferous sysrem. Cour. East Iran, Geol. Sura. Rep", v. 6, pp. 55-57, Tehran. Forsch. Senckenb.,v. fiA, pp. 1-345, Frankfun-am-Main. Fiùgel H. (1961) - Receptaculites neptuni DeÍr. 1827 from the Campbeli K.S.\7., Brown D.A. & Coleman A.R. (1983) - Am- Upper Devonian of Kuh-e-Shotori, East Iran. Bull. Ira- monoids and the correlation of the Lower Carbonife- nian Petrol. Inst., v. 4, pp.75-81, Tehran. rous of eastern Australia. Alcherínga, v.7, pP.75--123, Furon R. (1941,) - Géologie du plateau Iranian (Perse-Afghani- Sydney. stan-Béloutchrstan). Mém. Mus. Nat. Hist. Nat., v. 7, pp. Clar.rsen C.D., Korn D. & Luppold F..!l. (1990 - Litho-und 177-414, Paris. [not sighted]. Biofazies des mittle-bis oberdevonischen Karbonatprofi- Gansser A. (1955) - New aspects of the geology in Central les am Beringhauser Ti.rnnel (Messinghauser Sattel, Nor- Iran. 4th tù/orld Petroleum Congress Proceedings, Sec- dliches Rheinisches Schiefergebirge). Geol. Palàont., tion L/A5, v. 2, pp. 27930a, Carlo Colombo Publisher, \Y/estfulen, v. 18, pp. 7-6, Munster. Rome. Conil R., Groessens E., Laloux M., Poty E. & Tourneur F. Gutschick R.C. & Sandberg C.A. (1991) - Late Devonian hi (1991) - Carboniferous guide foraminifera, corals and story of Michigan Basin. In: P.A. Catacosinos 8c P.A. Jr. Deaonian-Carboniferous Conodonts from lran

Daniels (ed$ Early sedimentary evolution of the Michi 'SVorld, Australia, Indian subcontinent, South A{rica, gan Basin. Geol. Soc. Am. Spec. Pap., v. 256, pp. I81.-2A2, South America, and North Africa. Inst. Geologico y New York. Minero de Espàna, v. 2, pp. 367-372, Madrid. Heciin S.A. (1923-27) - Eine Routenaufnahme durch Ostper- Mawson R. Er Talent I.A. (1997) - Famennian-Tournaisian co- sien. Stockholme. fnot sighted] nodonts and Devonian-Early Carboniferous transgres- Higgins A.C. (1975) - Conodont zonation of the late Viséan sion and regressions. Geol. Soc. Am. Spec. Pap., v. 321., 'Westphalian and early strata of the south and central pp. 17 9-223, Boulder, CoÌorado. Pennines of northern England. Bull. GeoL. Surv. Gr. Odin G.S. (1988) - Green Marine Clays, Oolitic Ironstone Brit.. v.55, pp. 1-90, London. Facies, Verdine Facies, Glaucony Facies and Celadonite- Higgins A.C. (1985) - The Carboniferous System: Part 2 - Co- Bearing Facies - A Comparative Study. Dea. Sedim., v. nodonts of the Silesian Subsystem from Great Britain 45, 441. p., Elsevier, Amsterdam. and Ireland. In: A.C. Higgins & R.L. Austin (eds.) A Pander C.H. (1856) - Monographie der fossilen Fische des si- Stratigraphical Index of Conodonts: - Micropalaeontolo- lurischen Systems der Russisch-Baltischen Gouverne- gical Society Series, pp. 21A-227, E1lis Horwood Limi- ments. Akad. IViss., St. Petersburg, gi pp., St Petersburg. ted, London. Fartow Azar H. (1992) - Changhsingien Stage in east Iran. House M.R. (1981) - On the origin, classification and evolu- Discovery of genus ColanieLla and its biostratigraphic rion of the early Ammonoidea. In: M.R. House & J.R. importance. (In Persian with abstract in English). Geol. Senior (eds) The ammonoidea. The evolution, classifica- Suro. oflran, Geo Sciences, v. 1(3), pp.44-53, Tehran. tion, mode of life and geological usefulness of a major Perret M.E & \il/eyant M. (1994) - Les biozones à conodontes fossil gro,,rp. Syst. Ass., Spec., Y. 18, pp. 3-36. Academic du Carbonifère des Pyrénées. Comparisons arvec dautres Press Inc., London. régions du globe. fCarboniferous Conodont zones in F{r"rsseini M.I. (1992) - Upper Palaeozoic tectono-sedimentary the Pyrenees. Comparisons with zonations {rom other evolution of the Arabian and adjoining plates. lourn. parts of the worldl. Géobios, v. 27 (6), pp. 689-715, GeoL. Soc. London, v. 149, pp. 419-429, London. Lyon. Ji Q. & Ziegler \f. (1993) - The Lali section: an excellent Pollock C.A. (1968) - Lower upper Devonian conodonrs from reference section for Upper Devonian in south China. Alberta, Journ. Paleont., v. 42 (Z), pp 415-443, Tulsa, Cour. Forsch. Senckenb., v. 157, pp. 1-183, Frankfurt-am- Oklahoma. Main. Roberts J., Jones P.J. & Jenkins T.B.H. (1993) - Revised corre- Khalymbadzha V.G., Shinkaryov G.Y. & Gatovsky Y.A. lation for Carboniferous marine invertebrate zones of (1992) - New Famennian polygnathids (conodonts) eastern Australia. ALcberinga, v. 17, pp. 353-376, Sydney. from southern Kazakhstan. Paleont. Jour., Scripta Tèchni- Sandberg C.A. E{ Dreesen R. (1984) - Late Devonian icrio- ca, 1.992, v. 25 (2), pp. 69-81, New York. [Transiated dontid bio{acies models and alternate shallow-water co- from Novyye famenskiye polignatidy (konodonty) nodont zonation. Geol. Soc. Am. Spec. Pap., v. 196, pp. Yuzhnogo Kazakhstana. PaLeontologicheskiy Zhurnal, 1.43-17 8. Boulder. Colorado. 1"99I, v. 25 (2), pp.56-64, \fashingtonl. Sartenaer P. (i966) - Frasnian RhyncbonelLida from the Oz- Klapper G. (1997) - Graphic correlation of Frasnian (Upper bak-Kuh and Tabas regions (Eest lran). In: Contribu- Devonian) sequences in Montagne Norre. France, rnd tion to the Paleontology of E:rst kan, GeoL. Su.ro. Iran, western Canada. GeoL. Soc. Am. Spec. Pap., v. 321, pp. v. 6, pp. 25-54,Tehran. 113-1,29. Boulder. Colorado. Savoy L.E. & Harris A.G. (1993) - Conodont biofacies and Klapper G. & Lane R.H. (1985) - Upper Devonian (Frasnian) taphonomy along a carbonate ramp to biack shale basin conodonts of the Polygnathus biofacies, N. V. T., Can. (latest Devonian and earliest Carboniferous), southern- Journ. PaLeont., v. 59, pp. 904-951, Tulsa, Oklahoma. most Canadian Cordiliera and adjacent Monfana. Can. Kuz'min A"V. (1995) - The lower boundary of the Frasnian Journ. Earth 5c1., v. 30, pp. 24A4-2422, Ottawa. Stage in the Russian Platform. Stratigraplry and Geologi- Stòcklin J. 096I) - Lagoonal formations and salt domes in caL Correlation, v. 3 (3), pp. 304-313, Moscow. fTiansla- East lran. BulL. Iranian Petr" Instit., v. 3, pp. 39-33, Te- ted frorn Stratigrafiya Geologicheskaya Korrelyatsiya, v. 1 hran. (3), 1955, pp. 11I-120, Moscow.l Stócklin J., Eftekhar-Nezhad J. & Hushmand-Zadeh A. Lane H.R., Sandberg C.A. & Ziegler \í. (198b) - Taxonomy (1965) (reprinted, i991) - Geology of the Shotori Range rrnd nhvlosenv of some Lower Clrboniferous cono- (Tabas area, East Iran). Geol. Surr,. Iran, v.3, pp" 1,-69, donts and preliminary standard post-Siphonedella zona- Tehran. tion. Geologica et Pdlaeontologica, v. 14, pp. 117-164, Ssreet '{/. C. (1988) The Conodonta morphology. Taxo- Marburg. nomy, paleoecoiogy, .rnd er-oJr.rtionary hisrory of e long- Lane H. R. & Straka, I.I. 0974) - Late Mississippian and Ear- extrnct animal phylum. Oxford Monograph on GeoLogy 1y Pennsyivanian conodonts, Arkansas and Oklahoma. and Geophysics, v" 10, pp. 1,-291, Clarendon Press Ox- GeoÌ. Soc. Am. Spec, Pap., v. 152, pp. 1-130, Boulder, Co- ford, Oxford. ìorado. Taient j.A., Gaetani M., Mawson R., Molloy P. D. & Cona- Lemosquest Y., Conrad J. & Magner \f.L. (1985) - Ammo- ghan P. J. 0999) - Early Ordovician and Devonian (Gi- noids, North Africa. In: The Carboniferous of the vetian-Early Famennian) conodonts from the Karako- 200 M. Yazdi

rum and Hindu Kush, northernmost Pakistan. Rio. It. Ztegler \f. (1962) - Taxionomie und Phylogenie Oberdevonis- Paleont. Strat., v. 105, pp. 2Q1-230,Milan. her Conodonten und ihre stratigraphische Bedeutung. \falliser O.H. (1966) - Preliminary notes on Devonian, Lower Abh. Hessiche Landes. Bod.enforsclt., v. 38, pp. 1-166, and Upper Carboniferous goniatites in Iran. In: Contri- 'Wiesbaden. butions to the paleontology of East Iran. Geol. Surt;. Ziegler If. (1971) - Post-Symposium excursion, Sept. 15-18, Iran, v. 6, pp.7-24, Tehran. 1971,, to Rhenish Slate Mountains and Flarz Mountains, 'S7ebster G.D. (1969) - Chester through Derry conodonts and Fieid Trip Guidebook. Symposium on Conodonr Taxo- stratigraphy o{ northern Clark and southern Lincoln nomy, Marburg, Sept. 4-18, 1,971, Departmenr of Geo- Counties, Nevada. Unio. Calif, Publ., Geol. Sci., v.79, sciences, University of Philipps, 47 pp., Marburg. pp. l-121, Cali{ornia. Zíeg\er \f. (ed.) (1981) - Catalogue o{ Conodonts, IV. E. '\l'ebster G.D.& Groessens E. (1991) - Conodont subdivision Schweizerbart'sche Verlagsbuchhandlung, pp. 1-445, of the Lower Carboniferous. Cour Forsch. Senckenb., v. Stuttgart. i30, pp. 3 1-40, Frankfurt-am-Main. Ziegler !L Er Sandberg C.A. (19Sa) - Palmatolepsis-based revi- \Teddige K. (1984) - Z'.s,r Stratigraphy und Palaeogeography sion of upper part of standard Late Devonian conodonr des Devons und Carbons von NE-Iran. Senck. Letb., v. zonation. Geol. Soc. Am. Spec. Pap., v. 196, pp. L89-194, 65, pp. 17 9 -223, Frankfurt-am-Main Boulder, Colorado. Yazdi, M. (1999, ín press) - Late Devonian bioevents and sea Ziegler \W. Ec Sandberg C.A. (1990) - The Late Devonian level changes in East and Central lran and their poten- standard conodont zonation. Cour. Forsclt. Senckenb.. v. tial in discrimination of biogeographic patterns. Histori- 1.21., pp. 1-1 15, Frankftirt-am-Main. cal Biology.