Field Trip C CONODONT LOCALITIES in the SURROUNDINGS OF
Field Trip C
CONODONT LOCALITIES IN THE SURROUNDINGS OF GRAZ/STYRIA
By
Fritz EBNER Museum Joanneum, Raubergasse, Graz 11 figures, 8 tables and plates 15—16
A contribution to Project „Prevariscic and Variscic Events of the alpine mediterranean mountain belts"
Author's address: Doz. Dr. F. Ebner, Landesmuseum Joanneum, Abteilung für Geologie, Paläontologie und Bergbau, Raubergasse 10, A-8010 Graz, Austria.
101 100 Introduction The Paleozoic outcrops in the surroundings of Graz (approx. 1000 km2) are part of the Upper Au- stroalpine nappe system. It rests tectonically upon a crystalline basement („Altkristallin") and its Me- sozoic (?) cover. Parts of the Graz Paleozoic are overlain by Upper Cretaceous sediments, the so-called „Kainach Gosau", and towards the south-east by Tertiary deposits of the Styrian Basin. Structurally, it is characterized by nappes of probably alpine origin. According to H. W. FLÜGEL 1972 the Graz Paleozoic can be divided into three facies realms (fig.l): 1. Rannach facies 2. Hochlantsch facies 3. Tonschiefer facies (Schöckel Lst. facies).
Fig. 1: Facies distribution of the Graz Paleozoic (H. W. FLÜGEL 1972). Numbers indicate stops during ECOS Il-field trip C. An additional but stratigraphycally less well defined facies is known around Laufnitzdorf and Brei- tenau („Dornerkogel Group"), north of Frohnleiten.
102 Rannach- and Hochlantsch facies temporarily represent shallow water deposits and thus contrast with the Tonschiefer facies interpreted as basin sediments. The fundamental framework of Paleozoic stratigraphy within the Eastern Alps has first been establi shed in the vicinity of Graz. The geologic history dates back to 1828 when M. ANKER recognized the „Übergangsgebirge" (= transition zone) of G. A. WERNER. F. UNGER 1843 discovered fossils which he compared with Devonian faunas from the Eifelian hills and the Harz Mt.; G. STÄCHE and K. A. PENECKE successfully subdivided the rock sequence by means of fossils and established a first biostra- tigraphic scheme. Graz is also the place where F. HERITSCH lived and lectured as Head of the Department of Geolo gy at the University. He intensively studied coral and brachiopod faunas which were derived from the
Rannach facies transitional facies Hochlantsch fac.
Westfalian CO o Dult Fm. cc Namurian B ©©© LU llllllllllllllllllllllllll S U_ A z /Upper .(g)©©* O CD Visean Sanzenkogel < Fm. Ü Tournaisian
Famennian Höllerer - Kogel Lst. Li mestones & shales Frasnian at. 7 Platzl-Kqgel 9 * # P Givetian Hochlantsch\ ^_G_roup__/? FJfeUa_n_ faubenhalt Beds z Dalejan o Zlichovian > LJJ Dolomite Sandstone Fm. Q Pragian Kalkschiefer Fm.
Lochkovian Pridolian < Eggen- 3 Ludlovian feld CO
Fig. 2: Stratigraphy of conodont bearing sequences in the Graz Paleozoic (F. EBNER et al. 1979). Note that the rela tion of the Silurian sequence at Eggenfeld and the Laufnitzdorf Fm. with regard to the Rannach facies realm and the Hochlantsch facies realm respectively have not been solved yet. Studies in progress; conodonts can be expected from various levels • moderate or rich abundance of conodonts o low frequency of conodonts and bad preservation respectively 1—6 vertical range of the sections visited.
103 fossiliferous Middle Devonian limestones. His results are compiled in „Stratigraphie der geologischen Formationen der Ostalpen" published in a few copies in 1943. After World War Two study of lithology and fossils continued, this time by H. W. FLÜGEL and his students. In the fifties conodont research was initiated in the Eastern Alps by H. W. FLÜGEL and W. ZIEGLER by a study of the Upper Devonian Steinberg Lst. (1957). Conodont activities proceeded in the following years but were concentrated on limestones of Upper Devonian and Lower Carboniferous ages within the Rannach facies (A. KHOSROVI-SAID 1962, G. FLAJS 1966, M. G. KODSI 1967, L. NÖSSING 1974 a, b, 1975, L. NÖSSING, F. EBNER & H. W. FLÜGEL 1977, R. SURENIAN 1978, F. EBNER 1976 a, 1977 a, b, 1978, M. F. BUCHROITHNER 1979). The youngest strata of the Rannach facies comprise a shale and limestone formation, known as Dult Fm. Very recently, its Upper Carboniferous age has been proved by conodonts (F. EBNER 1975, 1976 a, 1977 a, b, 1978). To a lesser extent conodont research has been carried out in older rocks, although Upper Silurian and Lower Devonian conodont faunas have been described from various localities in the Rannach fa cies, from Laufnitzdorf, and from Eggenfeld (O. H. WALLISER in H. W. FLÜGEL 1961, O.H. WAL LISER 1964, H. W. FLÜGEL & H. P. SCHÖNLAUB 1971, F. EBNER 1976 b, F. EBNER et al. 1979). In recent years additional conodont data have been derived from Lower Devonian limestones which represent the transition from the Rannach facies to the Hochlantsch facies (M. F. BUCHROITHNER 1978, H. P. SCHÖNLAUB 1979, F. EBNER et al. 1979). Conodont information from the latter, how ever, is generally poor and, for example, comes mainly from Upper Devonian limestones. The conodont bearing horizons in the Paleozoic rocks around Graz are shown in fig. 2. Zon e
- Zon e
lowe r hermanni- varcus- cristatus
Icriodus brevis STAUFFER X Polygnathus cristatus HINDE X Polygnathus decorosus STAUFFER X Polygnathus dubius HINDE X Polygnathus of. latifossatus WIRTH X Polygnathus linguiformis linguif. d",cX, £.- MT X Polygnathus linguiformis parawebbi CHATTERTON X Polygnathus ovatinodosus KLAPPER & ZIEGLER X Polygnathus pseudofoliatus WITTEKIND X X Polygnathus timorensis KLAPPER, PHILIP & JACKSON X X Polygnathus varcus STAUFFER X Schmidtognathus hermanni ZIEGLER X
Tab. 1: Conodonts from the upper part of the Kanzel Lst.
104 1. Rannach facies
Within this facies conodonts are known which span the time from Upper Silurian to the Namurian/ Westfalian boundary level. To a great degree occurrences and abundance of conodonts are facies con trolled. The oldest formation of the Rannach facies, the Kehr Fm., comprises a 500 m thick sequence of shales/slates, sandstones and basic volcanites dominating the lower part („Untere Schichten von Kehr"), and a shaly-calcareous upper part („Obere Schichten von Kehr"). Conodonts are very rare. They were found in limestone lenses belonging to the upper part. The following conodont zones have been pro ved by H. W. FLÜGEL & H. P. SCHÖNLAUB 1970 and F. EBNER et al. 1979: ploeckensis-Zone: Oz. exe. inflata (WALLISER) siluricus-latialata-Zone: Oz. ziegleri WALLISER Oz. d.jaegeri WALLISER Lochkov: Oz. inch wurmi (BISCHOFF & SANNEMANN) Oz. r. remscheidensis (WALLISER) Sagittodontus cf. thuringicus JENTZSCH The Kehr Fm. is overlain by the 100 m thick Crinoid Fm. This formation includes different types of limestones, e. g., platy limestones, marly limestones, Flaser limestones and crinoidal limestones. So far, only Pandorinellina optima (MOSKALENKO) has been found indicating a late Lochkovian age (H. P. SCHÖNLAUB in H. W. FLÜGEL 1975). The Crinoid Fm. is succeeded by the 1000 m thick Dolomite-Sandstone Fm. which apparently re flects a peritidal environment with temporarily changing coast lines, sand barriers and small lagoons (A. FENNINGER & H. L. HÖLZER 1979). Yet, conodonts have only been found in normal marine contemporaneous deposits of the transitional facies. The Dolomite-Sandstone Fm. is followed by a thick shallow water limestone sequence, i. e., the fos- siliferous Barrandei Fm. of Eifelian age and the Kanzel Lst., which ranges from the Givetian to Frasnian. So far, only the Kanzel Lst. yielded stratigraphically important conodonts (M. F. BUCHROITHNER 1979). They belong to the lower varcus-Zone and the hermanni-cristatus-Zone (tab. 1). The shallow water limestones of the Kanzel Lst. are diachronously succeeded by nodular cephalopod limestones. Locally, this pelagic environment lasted through the whole Upper Devonian, the Lower Carboniferous, and parts of the Namurian stage (E2 ). Due to a significant facies break between Kanzel Lst. and Steinberg Lst. above the exact position of the Middle/Upper Devonian boundary has yet not been drawn satisfactorily. G. FLAJS who studied the presumed boundary level in great detail in a quarry (1966) did not recognize the hermanni-crista- £ws-fauna. Unfortunately, this section has been destroyed a few years ago. The cephalopod limestones on top of the Kanzel Lst. are subdivided into the 20—70 m thick Upper Devonian Steinberg Lst. and the 25 m thick Carboniferous Sanzenkogel Fm. Although this succession is conformable, locally a distinct disconformity with stratigraphic gaps, karst phenomena and reworked conodonts can be observed. Generally, the hiatus increases towards the east. For example, F. EBNER 1978 reported from here a gap from doII/IH up to cull/Ill. Contrary, in more western regions conti nuous sections across the Devonian/Carboniferous boundary have been proved. Studies of the microfacies and the fauna, geochemical analysis, and the occurrences of phosphatic nodules suggest that both the Steinberg Lst. and Sanzenkogel Fm. may have been deposited in depths between 60 and 300 m. According to M. F. BUCHROITHNER et al. 1979 the thicknesses of individual Upper Devonian co nodont zones depend on the amount of condensation and thus vary considerably. A list of conodonts from the Steinberg Lst. at its type locality has been published by R. SURENIAN 1978. Table 2 is ba sed on these data as well as on new information from section „Weihermühle" which both will be visi ted during the field trip. The Sanzenkogel Fm. can be subdivided into a lower member („Untere Sanzenkogel-Schichten") and an upper member („Obere Sanzenkogel-Schichten"). The first one, best exposed at Trolp Quarry reaches a thickness of 3,2 m, the latter approx. 22 m. According to L. NÖSSING 1974 b, 1975 and F. EBNER 1978 both members show the following thicknesses of Lower Carboniferous conodont zones at the type localities:
105 Tab. 2 THE CONODONT FAUNA OF THE STEINBERG LIMESTONE FORMATION
Ancyrodelia buckeyensis A. curvata A. lobata Icriodus curvatus I. sytmetricus Palmatolepis proversa P, cf. punctata P. subrecta P. transitans Polygnathus ancyrognathoideus P. asymmetricus ssp. P. pennatus P. varcus P. webbi P. sp. ex gr. xylus Ancyrodelia nodosa Ancyrognathus triangularis Icriodus alternatus I. cornutus Palmatolepis hassi Ancyrodelia gigas Palmatolepis gigas P. cf. subperlobata P. unicornis P. delicatula delicatula P. delicatula clarki P. minuta minuta P. quadrantinodosalobata P. subperlobata P. tenuipunctata P. triangularis P. circularis P. crepida P. glabra prima P. cf. regularis P. termini P. glabra acuta P. glabra lepta P. glabra pectinata P. klapperi P. marginifera ssp. P. minuta loba P.'perlobata perlobata P. perlobata schindewolfi P. pooli P. rhomboidea Polygnathus glaber glaber P. sp. ex gr. nodocostatus Icriodus nodosus Palmatolepis glabra distorta P. gracilis gracilis P. marginifera duplicata P. marginifera marginifera P. minuta schleizia P. quadrantinodosa inflexa P. quadrantinodosa inflexoidea P. quadrantinodosa quadrantinodosa P. cf. rugosa grossi P. stoppeli P. cf. stoppeli Polygnathus glaber bilobatus Bispathodus stabilis Palmatolepis perlobata helmsi P. perlobata sigmoidea P. rugosa trachytera Polygnathus communis communis P. margaritatus P. obliquicostatus Scaphignathus ? subserratus S. velifer Spathognathodus bohleanus Geniculatus claviger Palmatolepis glabra manca P. gracilis expansa —»• gonioclymeniae P. gracilis sigmoidalis P. rugosa postera Polygnathus granulosus P. styriacus Pseudopolygnathus brevipennatus P. dentilineatus Spathognathodus supremus Bispathodus aculeatus aculeatus B. aculeatus cf. anteposicornis B. aculeatus plumulus B. bispathodus B. costatus B. spinulicostatus B. ultimus B. ziegleri Palmatolepis gracilis gonioclymeniae Pseudopolygnathus marburgensis trigonicus Siphonodella praesulcata Protognathodus collinsoni p. kockeli P. meischneri
106 cu CQ 3 § •U to N fO -U Tab. 3 3 1 3 zone •^ »1 4J Öl QJ tO C 1 THE CONODONT FAUNA OF THE c nj c o tu tn -H H) 0 0 C 'S N 0 SANZENKOGEL FORMATION 3i U 'S 1 If) N r-l -U Q) ra 3 i
tj -W ancftoralis-zon e •O U) 0 0 ftj
0 3 «i J B 'S •S U) -zone sulcata-zone 0 tr> 0 3 4J 0 3 tt] •5 S D, » ftj T3 0 -H -zone to M •s H typicus-zone bilineatus a o bilineatus 01 4J CO 0 Ü 13
IM i U u l u ^ 1 U CD , CD 0) 1 tu tu i tu 3 1 CU 3 1 tt 0 1 tt 0 1 tt triangulus inaequalis- Pseudopolygnathus Gnathodus Gnathodus Gnathodus Siphonodella Scaliognathu s Gnathodus üp.A-zon e bollandensis 1 1 bilineatus Polygnathus communis communis P. communis ? P. purus purus P. purus subplanus Protognathodus collinsoni P. kockeli P. kuehni P. meischneri Pseudopolygnathus dentilineatus P. multistriatus Siphonodella praesulcata S. sulcata Spathognathpdus stablis Polygnathus communis carinus Pseudopolygnathus triangulus inaequalis P. vogesi Siphonodella duplicata Polygnathus bischoffi 3ispathodus aculeatus aculeatus Polygnathus cf. flabellus P. inornatus Pseudopolygnathus fusiformis P. triangulus triangulus Siphonodella obsoleta Elictojnathus bxalatus E. costatus J E. laceratus r Siphonodella cooperi S. lobata S. quadruplicata Polygnathus biconstrictus Pseudopolygnathus marginatus P. triangulus pinnatus Siphonodella cronulata S. isostica S, cf. isostica Dollymae sp. Gnathodus cuneiformis G. cf. cuneiformis Gnathodus antetexanus G. cf. antetexanus [— G. delicatus G. punctatus G. semiglaber Polygnathus vogesi Pseudopolygnathus nodomarginatus 1— Eotaphrus burlingtonensis Gnathodus commutatus homopunctatus G. hamatus G. isomescens G. syinmutatus symmutatus G. texanus G. typicus Hindeodella sogaformis Polygnathus orthoconstricta j Gnathodus commutatus commutatus G. sp. A G. commutatus lineatus G. bilineatus bilineatus Gnathodus girtyi ssp. Neoprioniodus montanaensis Spathognathodus campbelli Sp. werneri Gnathodus commutatus mononodosus G. commutatus multinodosus 1 G. commutatus nodosus Neoprioniodus scitulus Gnathodus bilineatus bollandensis J G. bil. bil. —*> bilineatus bollandensis
107 Siphonodella sulcata-Zone 35 crn Pseudopolygnathus tr. inaequalis-Zone 30 cm Pseudopolygnathus tr. triangulus-Zone 115 cm Siphonodella crenulata-Zone 105 cm Scaliognathus anchoralis-Zone 130 cm Gnathodus typicus-Zone 215 cm Gnathodus sp. A-Zone 400 cm Gnathodus b. bilineatus-Zone 150 cm Gnathodus comm. nodosus-Zone 960 cm Gnathodus b. bollandensis-Zone 300 cm Table 3 summarizes important conodonts of the Sanzenkogel Fm. The pelagic Sanzenkogel Fm. is disconformably overlain by the shallow water deposits of the Dult Fm. ranging in age from Namurian B to early (?) Westfalian. Limestone lenses intercalated in shales produced rare conodont faunas (table 4). Locally stratigraphic admixtures occur at the base of the Dult Fm.
Namurian' Westfalian B C|A
Table 4
Conodonts of the Dult Formation Faun a Idiognathoides Declinognathodus uppe r lowe r
Declinognathodus noduliferus Gnathodus glaber Declinognathodus lateralis Idiognathoides convexus Idiognathoides corrugatus Idiognathoides opimus Idiognathoides sinuatus Streptognathodus sp.
108 2. The transition from Rannach facies to Hochlantsch facies
During the last couple of years progress has been made to date the so-called „Kalkschiefer Folge" by means of conodonts. This formation comprises normal marine platy limestones, marly limestones, nodular limestones etc. which are regarded as time-equivalents of the peritidal Dolomite-Sandstone Fm. According to M. F. BUCHROITHNER 1978, F. EBNER et al. 1979 and H. P. SCHÖNLAUB 1979 the following taxa of late Lochkovian, Pragian and Zlichovian ages have been found: Belodella devonica (STAUFFER) Belodella resima (PHILIP) Icriodus latericrescens robustus ORR Icriodus s. simulator CARLS Pedavis pesavis (BISCHOFF & SANNEMANN) Icriodus ? postwochmidti MASHKOVA Neopanderodus sp. Ozarkodina exc. wurmi (BISCHOFF & SANNEMANN) Ozarkodina carinthiaca (SCHULZE) Ozarkodina r. remscheidensis (ZIEGLER) Pandorinellina st. steinhornensis (ZIEGLER) Pandorinellina st. telleri (SCHULZE) Pandorinellina st. miae (BULTYNCK) Polygnathus cf. gronbergi KLAPPER & JOHNSON Polygnathus I. linguiformis HINDE (gamma-morphotype) Lithologically, Middle Devonian rocks of the transitional facies are closely related to the Rannach fa cies realm, e. g., the Barrandei Lst. and dolomites with Amphivora. They are succeeded by Kanzel Lst. equivalents, as for example, the 80 m thick limestones on top of mountain „Platzl-Kogel" from wich a small and bad preserved conodont fauna of the varcus-Zone has been isolated recently (F. EBNER et al. (1979): Icriodus sp. Neopanderodus perlineatus LINDSTRÖM & ZIEGLER Polygnathus ovatinodosus ZIEGLER & KLAPPER Polygnathus pseudofoliatus WITTEKINDT Polygnathus timorensis KLAPPER, PHILIP & JACKSON Polygnathus sp. ex gr. linguiformis HINDE Polygnatus sp. ex gr. xylus-varcus In other places, e. g., the Höllerer Kogel, styliolinid bearing Flaser limestones of Givetian age have been found. The corresponding conodont fauna includes: Neopanderodus perlineatus LINDSTRÖM & ZIEGLER Polygnathus I. linguiformis HINDE (gamma-morphotype) Polygnathus sp. ex gr. xylus-varcus Finally, Upper Devonian (Frasnian) conodonts occur at locality „Platzl-Kogel". F. EBNER et al. 1979 published the following taxa which are derived from a limestone-shale-sequence: Ancyrodella buckeyensis STAUFFER Ancyrodella sp. Icriodus difficilis KLAPPER & ZIEGLER Icriodus expansus BRANSON & MEHL Icriodus nodosus (HUDDLE) Palmatolepis del. delicatulaBKANSON & MEHL Palmätolepis quadrantinodosalobata SANNEMANN Palmatolepis subrecta MILLER & YOUNGQUIST Palmatolepis triangularis SANNEMANN Polygnathus asymmetricus ssp. indet. Polygnathus decorosus STAUFFER Polygnathus ovatinodosus ZIEGLER & KLAPPER Polygnathus xylus STAUFFER Polygnathus sp. ex gr. xylus-varcus So far the Middle/Upper Devonian boundary plane has not been recognized in the transitional facies. 3. Additional conodont localities in the vicinity of Graz 3.1 Laufnitzdorf: O. H. WALLISER in H. W. FLÜGEL 1961 and 0. H. WALLISER 1964 identified a small Upper Si lurian to Lower Devonian conodont fauna which has been found in dark bituminous limestones inter calated in shales. The conodont bearing exposures are part of a tectonically very complex zone and thus make it difficult for precise assignments to any of the facies mentioned above. The fauna includes the following form-taxa of Pridolian and Lochkovian age: Ozarkodina ziegleri tenuiramea WALLISER Ozarkodina ortuformis WALLISER Icriodus sp. Ozarkodina cf. transitans (BISCHOFF & SANNEMANN) ramiform elements 3.2 Eggenfeld: Close to the village Eggenfeld north of Graz F. EBNER 1976 described an interesting section with a fairly rich conodont fauna. A 15 m thick dolomite-limestone complex which overlies diabases produ ced diagnostic conodonts of the siluricus- to woschmidti-Zones (table 5). In this section the conodonts are associated with other fossils, e. g., corals, crinoids, nautilids and brachiopods (Septatrypa subsecrata PLODOWSKI 1976). -Zon e Zon e -Zon e -Zon e -
siluricus latialata crispa eosteinhornensis-Zone woschmidti
Icriodus woschmidti ZIEGLER Kockelella variabilis WALLISER Ozarkodina ziegleri WALLIS ER Ozarkodina confluens (BRANSON &MEHL) Ozarkodina remsch. eosteinhornensis(WALL\SER) O.excavata excavata(BRANSON & MEHL) 0. remsch. remscheidensis (ZIEGLER) Ozarkodina snjadri WALLISER Polygnathoides emarginatus (BRANSON &MEHL) Polygnathoides siluricus BRANSON & MEHL
Tab. 5: Diagnostic conodonts from the dolomite-limestone horizon at the Eggenfeld section (after F. EBNER 1976).
110 Guide to Devonian and Carboniferous Conodont Localities
STOP 1. Section Weihermühle
STOP 2. Section Hartbauer
STOP 3. Trolp Quarry
STOP 4. Forstkogel („Open air-theatre" Quarry)
STOP 5. Hahngraben
STOP 6. Section NNE of Dult Monastery
During ECOS II-Field Trip C in the Graz Paleozoic those sections will be visited which belong to the Rannach facies. The excursion provides the opportunity to see the stratigraphic record from the Ancy- rognathus triangularis-Zone to the Gnathodus bilineatus bollandensis-Zone and even higher including strata dated as old as Namurian B. As mentioned elsewhere in this guidebook the Middle/Upper Devonian boundary has not been tra ced with such an accuracy which is needed for precise correlation. This is mainly due to a rapid facies change from shallow water carbonates to cephalopod limestones in the presumed boundary interval making it extremely difficult to find sections with diagnostic conodonts in either facies. The cephalopod limestone facies, lasting at certain places from the early Upper Devonian to the Gna thodus b. bollandensis-Zone (Namurian A) is subdivided into the Upper Devonian Steinberg Lst. and the Carboniferous Sanzenkogel Fm. Locally, these two formations are separated by a distinct uncon formity caused by local rises of the Devonian carbonate basin during an early stage of the Variscan oro genesis. This stratigraphic gap increases from west towards east with a maximum gap from marginifera- Zone to the Gnathodus b. bilineatus-Zone. Frequently, at the base of the Upper Sanzenkogel Fm. stra tigraphic admixtures can be found which correlate with the time of non-deposition. The reworked fau na consists of those elements which also have been found in the limestones below the unconformity plus those corresponding to the base of the overlying sequence. Interestingly, the missing column is ne ver represented by any reworked conodonts. Similar mixed conodont faunas can also be found as stratigraphic leaks. For example, at section Hart bauer stratigraphic leaks cut through the Steinberg Lst. almost from top to the base. The continuous section across the Devonian/Carboniferous bundary are located west of the river Mur. They are characterized by a) varying thicknesses of Upper Devonian conodont zones and b) by extremely reduced thicknesses of Tournaisian sediments. In these sections the base of the Up per Sanzenkogel Fm. is marked by a thin shale-chert-phosphorite layer. A second disconformity separates the Upper Sanzenkogel Fm. and the Dult Fm. In the section north of the Dult Monastery the Upper Sanzenkogel Fm. has been completely eroded. Hence, limestones of the Dult Fm. (Namurian B) conformably overlie the Steinberg Lst. The basal limestones of the Dult Fm. (= Dult Lst.) frequently contain mixed conodont faunas with elements referable to the correspon ding erosional surface. Study of microfacies suggests a shallow water environment for the Dult Lst. in which conodonts can hardly be found. This interpretation is supported by birdseye structures, occurrences of interstratal breccias and desiccation cracks. Laterally, the Dult Lst. passes into dark shales of the Dult Fm.; this horizon is associated in the shale sequence by hematite crusts. In the Rannach facies realm sedimentation ended in the uppermost Namurian or early Westfalian stages.
Ill @ © © ® Steinberg Sect.Weiher- Section Section NNE Section Area mühle Hartbauer Pult Monastery Hahngraben I si D 0 22 fc_9
IM — C £cö SCO
en CD • C CO 50 " i cc-1 :/-y- / Fig. 3: Stratigraphy of conodont sequences visited during the excursion. A Timing of stratigraphic admixtures L Timing of stratigraphic leaks • Reworked conodonts in mixed conodont faunas o Position of stratigraphic leaks Numbers: Thickness (meter) Fig. 4: Field trip stops in the Graz Paleozoic. 112 co CO conodont o _o C0§ c o o £ 5 c? zonation Formation lithology ü • o o— a o dominating E öl conodonts CO es co CO G.comm.nodosus- Upper 36 I! Gn.typicus-Zone Sanzenkogel Fm Q.O) |53|C ü. -IL Sc. anchoralis-Zone 34 costatus-Zone T .,., Tp P T^L iLUi 30 styriacus-Zone l~l~ 40 28 ? styriacus-Zone 3SI T< 38,39 37 velifer-Zone 26 rv ^^ i T 24 22 marginifera-Zone 20 T3 O O 18 =x Ol „LI 16 rhomboidea-Zone w 12 20 10 crepida- Zone Rtriangularis-Zone T=-T gigas-Zone ^/V-fC/^iy pzrDirrq transition =^§^ A>l--7.v,-, Kanzel Lst./ Ancyr.triangularis O CD Steinberg Lst. o ','i>\-V-V, o 1 Om a HUT T Middle Kanzel Lst. o Devonian Fig. 5: Steinberg Lst. at section „Weihermühle". 01 c Tab. 6 0 N 1 01 01 CO THE CONODONT FAUNA OF si •H H -H Q, 01 01 C Polygnathus sp. ex gr. xylus •— Polygnathus sp. Ancyrodella sp. Ancyrognathus sp. Icriodus sp. Palmatolepis hassi _ — P. proversa P. subrecta P. sp. __ Polygnathus webbi Ancyrognathus triangularis Ancyrodella curvata A. buckeyensis A. lobata Palmatolepis cf. gigas P. sp. ex gr. hassi-gigas P. gigas Ancyrodella sp. ex gr. lobata-curv. Palmatolepis subperlobata P. tenuipunctata P. quadrantinodosalobata P. minuta minuta P. crepida P. termini P. circularis P. cf. circularis P. glabra prima P. minuta lona P. klapperi P. glabra lepta P. glabra sp. Polygnathus sp. ex gr. nodocost. Paimatolepis glabra pectinata P. rhomboidea P. glabra acuta Polygnathus glaber glaber Palmatolepis glabra distorta P. stoppeli P. quadrantinodosa quadrantinodosa P. minuta schleizia P. marginifera ssp. P. marginifera marginifera P. perlobata schindewolfi P. gracilis gracilis P. perlobata helmsi P. rugosa trachytera Scaphignathus ? suhserratus "Spathognathodus" sp. Pseudopolygnathus sp.sp. Polygnathus styriacus P. gracilis expansa —^gonioclymeniae Pandorinellina ? sp. Palmatolepis gracilis sigmoidalis "Spathognathodus" bohleanus P. gracilis sp. Bispathodus bispathodus Polygnathus communis communis Bispathodus stabilis B. aculeatus aculeatus B. costatus Pseudopolygnathus cf. brevipennatus Bispathodus spinulicostatus Pseudopolygnathus dentilineatus P. ? sp. Scaliognathus anchoralis Hindeodella segaformis Gnathodus delicatus G. antetexanus G. cuneiformis G. isomescens Pseudopolygnathus triangulus ssp. Palmatolepis gracilis gonioclymeniae Gnathodus typicus G. texanus G. hamatus 114 c 0 1 •Hw IIa,I IIuI tl "< a u -4 --H 31 t! 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 115 STOP 1. SECTION WEIHERMÜHLE Kanzel Lst. — Steinberg Lst. (Ancyrognathus triangularis-Zone — costatus-Zone) — stratigraphic gap —. upper Sanzenkogel Fm. (Scaliognathus anchor-alis-Zone — Gnathodus c. nodosus-Zone). In this section the Middle/Upper Devonian boundary has not been traced by conodonts yet. This is mainly due to a significant facies change occuring at this passage. Biostratigraphically, section Weihermühle starts in the A. triangularis-Zone. In the succeeding pela gic Steinberg Lst. several Upper Devonian conodont zones have been recognized. They show the follo wing thicknesses: . Conodont Zone minimum thicknesses maximum thicknesses (cm) _ _ ;, (cm) Gnathodus typicus— 400 Scaliogn. anchoralis-Zone 70 costatus-Zone 220 '(+70) styriacus-Zone 300 (+70) ? styriacus-Zone 130 velifer-Zone 140 (+ 140) marginifera-Zone 520 (+340) rhomb oidea-Zone 620 (+ 290) crepida-Zone 350 (+90) triangu laris-Zone 100 gigas-Zone 240 (+70) A. triangularis-Zone 320 (+70) The Steinberg Lst. are conformably overlain by the lithologically very similar» Upper Sanzenkogel Fm. which have been dated — at this locality — as old as the Scaliognathus anchoralis-Zone. Hence, both formations are separated by a disconformity. At the base of the Sanzenkogel Fm. reworked conodont faunas have been found. The sectioo,with in the Sanzenkogel Fm. is badly exposed.' In the uppermost beds conodonts of the Gn. c. nodosus-Zo ne have been identified. . „ ...... Field notes: Red numbers are sample numbers as indicated in fig. 5. Recommended samples: Ancyrognathus triangularis — costatus-Zone. STOP 2. SECTION HARTBAUER ; Kanzel Lst. — Steinberg Lst. (dol — marginifera-Zone) — gap — Upper Sanzenkogel Fm. (Sc. ancho ralis-Zone — Gn. b. bollandensis-Zone) — Dult Fm. with Dult Lst. (with Declinognathodus-Idiognathoi- des fauna), and Dult Shale (Namurian C — ? Westfalian). In this section too, at the base of the Steinberg Lst. a distinct facies break occurs. So far, the Stein berg Lst. section which may reach a thickness of some 20 m has not been studied in great detail. It's uppermost beds contain conodonts of the P. marginifera-Zone. They are conformably overlain by the Upper Sanzenkogel Fm. which has been dated as 5c. anchoralis-Zone at the base. Also, reworked fau nas (stratigraphic admixtures) have been found in a 2 cm thick horizon at the base of the Upper San zenkogel Fm. This mixed fauna contains conodonts of the P. marginifera-Zone and the overlying stra ta of Tournaisian age. Stratigraphic leaks have been found too occuring from the unconformity through the Steinberg Lst. almost.to the boundary between Kanzel Lst. and Steinberg Lst. Recognition of the se phenomena, however, is extremely difficult. The Upper Sanzenkogel Fm. reaches a thickness of approx. 22 m. Near the-base lydites have been found. The uppermost part have yielded conodonts belonging to the Gn. b: bollandensis-Zone. Uncon- formably, they are followed by the Dult Fm. with 5 m thick Dult Lst. at the base. These limestones, in turn, are separated from the shales above by a disconformity which is marked by hematite crusts. In the Upper Sanzenkogel Fm. conodont frequency varies considerably. In particular, this is true for the interval between the Gn. typicus and Gn. b. bilineatus-Zones during which conodont abundance is very poor. Those conodonts which have been found are very small and also, very thin; they are descri bed as Gnathodus sp. A. Gnathodus sp. A: Small asymmetrical cup (platform) with an acute posterior end. In oral view the platform may be smooth or ornamented by few nodes. The inner part of the platform bears a short and low parapet. 116 ginal samplenumbershav e beendestroyed lowing conodontshavebeenidentified: sulcata-Zone conodonts ne sequence. thick shale-chert-phosphorite-intercalation occurswithi down sectiowhich D: C: Base tus-Zone cording and theDultLst.(GnathodusspA-Zon X: Mixedconodontfaunas. E: Base B: A: Boundaryhorizon Top Pseudopolygnathus micropunctatusBISCHOFF Polygnathus communisBRANSON Top The typsectionwasfirs t established Polygnathus styriacusZIEGLER Palmatolepis perlobata Palmatolepis The typsection Spathognathodus stabilis(BRANSON Trolp quarry Spathognathodus tridentatus(BRANSON) Steinberg Lst.(P.styriacus-Zone,B.costatus-Zone,Protognathodus-Fauna);SanzenkogelFm(Siph. References: Recommended samples:UpperSanzenkogelFm. Red numbersindicatesamplewithin Red marks: In DEVONIAN CARBONIFEROUS the of of to of of Middle Upper Dinantian Silesian and followingDultLst.twospecimensbelongin i/m 3ZT SteinbergLst. UpperSanzenkogelFm. of W T Dult UpperSanzenkogelFm. N T V H.W. FLÜGEL& B A C thepassagfromDevonia n — ends G. bi Scaliogn.anchoralis Declinognathodus- gracilis Lst. is Gn. typicus-Zone). P.marginifera 1 thetyplocalityofPolygnathusstyriacusfirstdescribed in i neatusbol Idiognathoides of is the F. Kanzel Lst./Steinberg theLowerSanzenkogelFm.islocated represented EBNER1976 Gn.typicus-Zone. ULRICH &BASSLER landen - SIS W. MÜLLER ZIEGLER -r~i- strat.admixtures -TWE\ ~I~,5I~M >^'\- I I I I I by I I I .11 ID I stratigraphic GAP /I-. STOP •* (0 2 & MEHL coarsebeddedmicriticFlaser-limestonesbegin a, the GAP by I IIC & MEHL) 1977 I — and L. At 1957 UpperSanzenkogelFm.drawn 3. 1 1 to A Lst. Gn. NÖSSING 1974 TROLP QUARRY Lower Upper a, the lost, the b. Kanzel Steinberg Dult in Sar 1977 izenkogel Fm. & Fm. Carboniferous, Lst. Lst. bilineatus-Zone). the base a ZIEGLER to restudyhasbeenstartedwhic h concentrates b, northernwall c. mononodosushasbeenobserved. b. bollandensis, The Visean/Namurianboundaryshould Idiognathoidesopimushavebeenfound. and to Gn. a subspecieslevel, distinct changes placed abovethislevel. has beenrecognized interval withdecreasedconodontabundance form). the Sanzenkogel Fig.6: c. nodosus-Zone). Gn. which ness aboveequivalent of the 1978. During an theScaliognathusanchoralis-Zone commutatusandSp.campbelli(LowerGn. inthe Stratigraphy more are Interestingly,within A—E: b. a, almostsmoothouterpar b, the bollandensis(moreslenderplatforms and in characterized or eastface red 1975. of the range lessuniformdevelopedlimesto also,acrosstheTournaisian/Vi - fieldmarks. a theabondonedquarry ofthe limestonebetween of Fm.are Due i. by secondoccurrence in of section of in e., fig. W.ZIEGLER to to Gn. a thequarry.Thupsid fromGn. bythe The horizon conodontfaunas the cu 7. c.nodosus „Hartbauer". characterized the Hlß/gamma fact,thathisori highestparts in occurrences of range theB.costa b. of the 6 bilineatus a 1957. the a m of the of second thick lydite be 20 strata plat Gn. by Gn. on fol 117 on Ac of of cm 00 • QJ C 0 ' O 0 §0) N 0 «1 3 W N 01 , W 0 0) 3 R SD odosus-zon e • q q Q 0 | C N | q 3 i 3 arg 1 q 01 g 3 3 . q SECTION HARTBAUER- 0} 3 UPPER SANZENKOGEL FORMATION •q 1 Ul -Q 3A Qi n ^1 !i 15 or 3 n3 Palmatolepis glabra pectinata P. glabra prima P. gracilis gracilis P. marginifera marginifera P. minuta minuta Polygnathus glaber bilobatus Palmatolepis glabra distorta • P. glabra lepta Gnathodus antetexanus —• i -•» — G. punctatus 1 G. typi cus - Hindeodella segaformis Polygnathus communis communis P. cf. communis carinus Pseudopolygnathus triang. pinnatus Scaliognathus anchoralis Siphonodella sp. Gnathodus cuneiformis •v — •_.. G. delicatus G. semiglaber - ;. _ M, Polygnathus inornatus — «••» P. orthoconstrictus 1 F. sp. Gnathodus texanus ^— G. sp. — . wmm mm — _ —mm G. cf."texanus ^^^— G. symmutatus symmutatus ^— ^— G. commutatus cf. commutatus — G. sp. Ä Spathognathodus sp. ' Gnathodus commutatus commutatus G. bilineatus bilineatus — _ — — Neoprioniodus montanaensis Spathognathodus campbelli _— __ _ Sp. werneri —» •— •- G. bilineatus cf. bilineatus MB G. girtui ssp. ~~ i G. commutatus lineatus *""" I ' G. commutatus nodosus G. commutatus mononodosus ,1 llj —-I '' . G. commutatus homopunctatus 1 , Neoprioniodus scitulus ^— Gnathodus -.bilineatus MI.—^ J?il.. boll >^— _ ••- ^~ G. bilineatus bollandensis ^~ — ' G. bilineatus ssp. mmmm ,, «__ tmmmm • G. commutatus multinodosus 1 Fig. 7: Stratotype of the Upper Sanzenkogel Fm. c \ Stratotype Upper Sanzenkogel Formation at section „Hartbauer". 10 m \ ati o 3 E z sean boundary. Another goal has been to o \ | _ l s check whether Dinantian conodont zona- o — \ s O 10 LL CC \ f j atio n on t tion based on the genus Siphonodella (Ch. ^ w 5 Declinognath.- \ ill I £ 5 Idi ogna tfioi ctes-\ ™ ^ — I S § A. SANDBERG et al. 1978, 1979) can be Q © 22 used to subdivide rocks of this age. Finally, For«. z (i) Em «* a campaign to collect cephalopods is plan .•I 52 o ®i!® Os""c. m Gnä thodus m Foram. 51 ned for the future. Thus, data shown in fig. Crin. 50 tioii a nden s i s - cc | ; : 20 8, tab. 8 are only preliminary to demonstra < «T C> i 49 1 48 te our present knowledge of this important < Z —°~s < i 47 i_ L section. • ! CC - - 3 Distribution of the genus Siphonodella is o cc S " 44 {*/ restricted to certain beds. This fact makes it UJ 43 . — z 42 difficult for use of the zonatian based on si- if i 12 phonodellids, in particular, across the Devo 3 40 CO nian/Carboniferous transitional beds and i. 39 16 L U within the interval from the Siph. sulcata- J O Zone to the Ps. tr. inaequalis-Zone (Sioh. CO X 38 1 :". duvlicata to Sioh. sandbergi-Zone). upper 3 Gnathodus Due to rare occurrences of Sioh. sulcata nodosus- u. ':•'. in this section the Devonian/Carboniferous o 3 T Crtn. 37 boundary is drawn above a 15—20 cm thick DC horizon which is dominated by representa tives of the genus Protognathodus and be — 12 UJ II < ) low the appearance of Pol. vurus subplanus QJ c U. 33 and Pol. p. purus. Interestingly, in this sec lower • 11 z tion the genus Siphonodella has also been - Zone o < found in the lower Sc. anchoralis-Zone. 3 10 32 z LU 31 Field notes: Red numbers are (A 30 c o I -3 29 sample numbers corresponding to fig. 8. 0) o • Gnathodus IB > bilineatus Crin. 00 27 N s bilineatus- s 8 Recommended samples: Zone .1 ¥ 26 —1ZIZZ~_ Upper B. costatus-Zone; Protognathodus- cc 25 _-_ 1 Fauna — Upper Siph. crenulata-Zone; Sc. i •« < 20 anchoralis-Zone; Gn. typicus-Zone. :-© 19 Sa n rr_: 6 o =-© I sp. A.- References: H. W. FLÜGEL & Zone W. ZIEGLER 1957, L. NÖSSING 1974 a, j > Brachiop. IT a 1 16 b, 1975. i— • 14 3 Ostrac. 4 u. 3 13 Ostrac. 12 n UJ | I J_ Gna thodus typic-us- Q. 5 j 1 gg 11 — 3 o g 6 J~ 6 A Scaliognathodus S 4 3 2 3 1 0 Foram. 0 z Palmatolepis «) © Cephalop. marginitgra - J <• i_i Zone • © blackish < D 0 Conodonts z z © dark gray per z 3 1-10 s o © light gray B 1,5kg(appr) >rownish JJJTj * > < € ® yellowish -1 10-25 UJ •k >25 CO D G) or« nga-y •1 ow H 119 Tab. Hindeodella segaformis G. typicus Gnathodus texanus Spathognathodus stabilis Scaliognathus anchoralis G. semiglaber Siphonodella crenulataMT S. quadruplicata TROLP QUARRY- THE CONODONTFAUNA G. isomescens Gnathodus cuneiformis Gnathodus antetexanus Siphonodella isostica Pseudopolygnathus Polygnathus communiscarinus Siphonodella crenulataMT Polygnathus cf.flabellus SANZENKOGEL FORMATION Siphonodella lobata G. delicatus Dollymae sp. P. 'Pseudop. marburgensistrigonicus Gnathodus cf.antetexanus P. Pseudopolygnathus fusiformis Polygnathus biconstrictus S. sp. Bispathodus aculeatus S. duplicataMT S. cf.isostica Siphonodella duplicata S. obsoleta Siphonodella cooperiMT Pseudopolyg. triangulus Polygnathus bischoffi Siphonodella sulcata P. Pseudopolygnathus multistriatus P. Protognathodus collinsoni Siphonodella praesulcata P. B. Bispathodus costatus P. P. Polygnathus purussubplanus P. P. P. Polygnathus communis Spathognathodus supremus P. Palmatolepis triangulusssp. marginatus ultimus sp. purus gracilissigmoidalis sp.exgrprimus-dentilineatus dentilineatus meischneri kockeli communis gracilisgonioclymeniae 8 triang. ? gracilis 1 OF pinnatus sensu HASS 2 2 1 1 2 .q o •H •a 4J C m 0 Ol 4J -H .q +J lH 10 (0 c ID 0 C CD 1 N H "*"• q q • — ti bi'H« H Vft -q 'H -q "o -H M tj CH 13 45 -U faltjCD to illH tl S ft qSCD 0 e 0 CD 'H, 10 CD 3 10 O -H+J fal 10 3 1 10 «1 0 ft 31 TH '-HSCD -Q H CD -H C 01 10 M toi 1( Ol| N .q —«• 10 1 • CD . fai "H ON jq i ~4 r-t Co M CD 0 10 O !H C CD . —• ^"^ 10 10 10 c CO 1 N C q 0 3 3 0 t3 ItJ-~f-U ••H J5 to M .q ~H 16 78 to ft ou a q --IH O CD 10 •-( 3Ü t3 •N il x: i •-i l^i — •— to i Ü — O N q o O C CD 10 0] 0 ft CD CD H Q, io 3 a in 1 q ft CD "•H to 0) CD q ft ft M D 3 . — "™™ M 10 10 C CD 1 19 20 H •H -q •q -u to 3 Ü 0 to CD Ü 10 q 10 01 10 q N O C 0 fa. — ral. 21 x; -i-l U •3 •u 4J q O 10 O 3 01 31 Q, 3 to C CD N 0 1 CARBONIFEROUS UPPER Visean Tournaisian DEVONIAN Sanzenko g e 1 Fm. Steinberg Lithology/Thickness Upper lyd ! Lower Lst. S ħ +-» ~ o O o CO E CI o CO o S E CD Fig. 3 limestones — s 1- 8: z 2 0 l; Stratotype t ^y s\j — — • — — — — — — i— i— i"' i "i r ^^ _ —•_ r^y r^/ _ _ — — _ srxz. r^j (in — — />-/ _•— _ — _ — — ______r*-* — — — —- — of m) S^J _•—_ — the /-v> _»— r*-/ Samples LowerSanzenkogel — r* r> S*sS r^/ _a_ -2 - - ^10 EV3-9 ------16 -13 - 1 20 2 12 1 15 14 18 17 19 21 -Protognathodus Rtriancj.inaequalis upper costatus Pseudopolygn. Pseudopolygn. triang.triang. upper triang.triang.- S.sulcata- lower Conodont crenulata crenulata Gnathodus Fm. Siph. Seal Siph. at anchoralis Trolp iognath Quarry. Z F.- - .0 typicus Siph. S.sulcata Siph.sandbergi- S. n Siphonodella crenulata upper lower praesulcata crenulata ation us S.duplicata isostica sandbergi Siph. Siph. - STOP 4. FORSTKOGEL („Open air-theatre" Quarry) Steinberg Lst. and Sanzenkogel Fm. (Upper Devonian, Lower Carboniferous). The Forstkogel is the classical locality for the Steinberg Lst. development. In this area, however, the re is some lack of.good exposures but even worse is the complex tectonic which affected all rocks. Ac tually, it is impossible to demonstrate in one single section a continuous sequence of Upper Devonian strata. According to R. SURENIAN 1977 thicknesses of certain conodont zones vary considerably within short distances; locally, due to strong currents, some conodont zones are even missing (M. F. BUCH- ROITHNER et al. 1979). During the last century in the Forstkogel area the colored cephalopod bearing Steinberg Lst. was ab undantly quarried. The rocks became famous all around Graz for use as building material. Today the quarries are mostly used for recreation purposes or sporting sites of a nearby nursery school. The tectonically complex structure of the Steinberg Lst. and the Sanzenkogel Fm. at this stop is de monstrated in fig. 9 (R. SURENIAN 1977). In this figure the tectonic of the quarry „Open air-theatre" (Freilichtbühne) is also shown. In some cases isoclinal folding was so strong to produce normal and up side down sequences of lithologically similar Steinberg Lst. and Sanzenkogel Fms. Fig. 9: Tectonic sketch of the area around Forstkogel; square indicates the open-air theatre quarry (according to R. SURENIAN 1977). 1—4: Steinberg Lst. 5—6: Sanzenkogel Fm. 1: P. marginifera-Zone 5: cu I 2: P. velifer-Zone 6: cull 3: Pol. styriacus-Zone 4: B. costatus-Zone (A) In the northern wall of the quarry the P. marginifera-Zone has been proved reaching a thickness of more than 6.00 m; also, the B. costatus-Zone with a thickness of 3.00 m has been found. Yet, veli fer-Zone, styriacus-Zone and the Protognathodus-Fauna have not been recognized. The normal sequen ce of this section ranges into the Gn. typicus-Zone. This horizon is tectonically overlain (overfolded) by an upside down sequence of the Sanzenkogel Fm. plus Steinberg Lst. as illustrated in fig. 9. Within the 5c. anchoralis-Zone a thin phosphorite bearing shale horizon has been found in the nor mal sequence. (B) In the southeastern part of the quarry the Pol. styriacus-Zone is represented by limestones of more than 4.50 m thickness; in addition, the B. costatus-Zone has been proved in limestones of more than 7,50 m thickness. (C) In the north-western corner of the quarry the following zones have been recognized in normal order: marginifera-Zone: more than 3.00 m thick 122 velifer-Zone: 3.70 m thick styriacus-Zone: more than 3.70 m thick costatus-Zone: more than 2.50 m thick. (D) In the gorge which leads to the quarry limestones of the Pol. styriacus-Zone have been found in the northern part; in the southern part of the gorge equivalents of the B. costatus-Zone occur. Caused by karst, at this place the Flaser-limestones are deeply excavated and porous. They are re-fil led by red soils of Plio- and Pleistocene ages. Conodonts have been discovered in these soils indicating the residual nature of the soil. According to R. SURENIAN 1977, for example, from 3 kg of soil a mi xed conodont fauna composed of 71 single elements has been isolated. They span the time from basal Famennian to the Gattendorfia Stage. Preservation of the conodonts is relatively good. Field notes: Red letters A to D indicate the location of the sections mentioned in the guide book. References: R. SURENIAN 1977, 1978, M. F. BUCHROITHNER et al. 1979, H. W. FLÜGEL & W. ZIEGLER 1957, H. HOLLER 1958. STOP 5. HAHNGRABEN Steinberg Lst. (P. marginifera-Zone) — stratigraphic gap — Upper Sanzenkogel Fm. (Gn. b. bilinea- tus-Zone to Gn. c. nodosus-Zone) — stratigraphic gap — Dult Lst.(Declinognathodus-Idiognathoides- Fauna). The yellowish micritic Steinberg Lst. yielded conodonts of the P. marginifera-Zone. They are succee ded by the Upper Sanzenkogel Fm. which here begins in the Gn. b. bilineatus-Zone. Hence, both for mations are separated by an unconformity assuming a stratigraphic gap. The Upper Sanzenkogel Fm. consists of light grey, in part clayey and bedded limestones of a thickness of 7.60 m. They are overlain by black Dult Lst. of 6.00 m thickness. Dult Lst. and Upper Sanzenkogel Fm. are also separated by a disconformity. At the base of the over lying Dult Lst. reworked conodonts have been found. They represent diagnostic elements of the Stein berg Lst. and the Upper Sanzenkogel Fm. Sedimentologicalcriteria such as desiccation cracks and breccias are in good accordance with the co nodont data which imply a distinct disconformity. In samples from the base of the Upper Sanzenkogel Fm. Upper Devonian conodonts of the under lying Steinberg Lst. have been found, i. e., Palmatolepis sp. They occur as high as 1.80 m above the dis conformity. The Dult Fm. too contains mixed conodont faunas and in situ faunas; the latter belong to the Namurian B (= lower Declinognathodus-Idiognathoides-Fauna). Furthermore, conodonts of Up per Devonian, Visean, and Namurian A strata have been found which correspond with the lower limit of the disconformity. Field notes: Red numbers: 1. Top of Steinberg Lst.; 2. Approx. upper limit of the Gn. b. bi lineatus-Zone; 3. Top of Sanzenkogel Fm.; 4. Base of Dult Lst. Recommended samples: Dult Lst. with an in situ fauna of Namurian B age. However, frequency of conodonts may vary to a certain degree. In general, yellowish-brownish rocks produced richer faunas (mixed conodonts) than black micritic limestones. References : F. EBNER 1976 a, 1977 a, b, 1978. 123 Palmatolepis glabra lepta P. glabra pectinata P. glabra prima P. marginifera marginifera P. minuta minuta P. quadrantinodosa inflexa P. rhomboidea Icriodus sp. Palmatolepis sp. Cavusgnathus sp. Gnathodus bilineatus bilineatus G. bilineatus bollandensis G. commutatus commutatus G. commutatus homopunctatus G. commutatus nodosus G. typicus G. sp. Declinognathodus noduliferus Gnathodus glaber Idiognathoides corrugatus I. opimus STOP 6. SECTION NNE OF DULT MONASTERY Steinberg Lst. (P. marginifera-Zone to P. velifer-Zone) — stratigraphic gap — Dult Lst. (lower Decli- nognathodus — Idiognathoides-F anna). The yellowish and brownish micritic Steinberg Lst. with conodonts representing the marginifera- to velifer-Zone are overlain by coarse bedded dark Dult Lst. Both formations are separated by a distinct unconformity. Yet, this section is the only one known in which the Dult Lst. overlies the Steinberg Lst. Hence, we assume, that the Sanzenkogel Fm. has been eroded prior to deposition of the Dult Lst. This conclusion is supported by a nearby section with a thin horizon exhibiting the Sanzenkogel Fm. and, also, in section Hahngraben with mixed Upper Devonian and Lower Carboniferous conodont fau nas found in the basal Dult Lst. Section NNE Dult Monastery co v- Q3 co co "O CD TO o Os 03 c CD e co 03 O o o •o •Q .£ o co 03 CO 03 55 "O •2! co •§§ E JQ -2 r- C/3 N CO li- TO c ° -5 c C CO "m P •5 as CD C: O CD "& CD CD C C Q. CD v. i~ ° co CO -9? Q. 03 03 CO o g'ci 'S £ 03 i- CO CD CD c c T3 I >-. >~ •§.1 Q5< •Q -Q D) 6) O a o >-. 1^. -c 03 Q. co CD CD CD Q. Ci CD CD • • CD S E C o: Q: Q; O; CJ CD CD O. Q: Q: a; oo -A Scaphignathus velifer- Zone 1 • strat. Q leak v Rm. marginifera-Zone Fig. 11: Stratigraphy and conodont occurrences of section „NNE Dult Monastery". Numbers indicate red field marks. Furthermore, we draw attention to the fact that in sample no. 1 mixed conodont faunas (stratigra phic leak) occur; they belong to the P. marginifera- and Gn. b. bilineatus-Zonesl This is another proof for deposition of the Sanzenkogel Fm. on top of the Steinberg Lst. However, they have been comple tely eroded before sedimentation of the Dult Lst. began. Field notes: Red numbers: 1. P. marginifera-Zone; 2, 3: P. velifer-Zone; 4: Namurian B (lo wer Declinognathodus—Idiognathoides-Fauna). Recommended samples: Dult Lst., bed no. 4 with relatively abundant conodonts of the Declinognathodus—Idiognathoides-F anna.. Horizon between bed no. 2 and 3 with conodonts of the P. velifer-Zone. References: F. EBNER 1976 a, 1977 a, b, 1978. 125 References: ANKER, M. (1829): Erster Versuch einer Gebirgskarte von Steyermark. — Graz. BUCHROITHNER, M. F. (1978): Biostratigraphische Untersuchungen im Paläozoikum der Steiermark. — Mitt. naturwiss. Ver. Steiermark, 108, 77—93, 2 figs., 1 pl., Graz. — (1979): Das Paläozoikum von Tobelbad bei Graz. — Mitt. naturwiss. Ver. Steiermark, 109, 63—70, 1 fig., Graz. — , EBNER, F. & SURENIAN,R. (1979): Die Entwicklung der Steinbergkalke (Oberdevon, Grazer Pa läozoikum) an ihrer Typuslokalität. — Mitt. naturwiss. Ver. Steiermark, 109, 71—84, 3 figs., 6 tab., Graz. EBNER, F. (1975): Der Nachweis von Namur im Paläozoikum von Graz. — Anz.Österr. Akad. Wiss. Wien, math.-naturwiss. Kl., 1975, 119-125, Wien. — (1976): Die Schichtfolge an der Wende Unterkarbon/Oberkarbon in der Rannachfazies des Grazer Paläozoikums. - Verh. Geol. B.-A., 1976, 65-93, 3 figs., 4 pl., Wien (1976 a). — (1976): Das Silur/Devon-Vorkommen von Eggenfeld — ein Beitrag zur Biostratigraphie des Grazer Paläozoikums. — Mitt. Abt. Geol. Paläont. Bergb. Landesmus. Joanneum, 37, 4—33, 2 figs., 5 pl., Graz (1976 b). — (1977): Die Transgression der Folge der Dult (Oberkarbon, Paläozoikum von Graz). — Mitt. natur wiss. Ver. Steiermark, 107, 35—53, 4 figs., Graz (1977 a). — (1977): Die Gliederung des Karbons von Graz mit Conodonten. - Jb. Geol. B.-A., 120, 449-493, 1 fig., 3 tab., 6 pl., Wien (1977 b). — (1978): Stratigraphie des Karbon der Rannachfazies im Paläozoikum von Graz, Österreich. — Mitt. Österr. Geol. Ges., 69, 163-196, 7 figs., 4 tab., Wien. — , FENNINGER, A. & HOLZER, H.-L. (1979): Die Schichtfolge im Übergangsbereich Rannach-Fa zies — Hochlantsch-Fazies (Grazer Paläozoikum) im Räume St. Pankrazen — Großstübing. — Mitt. naturwiss. Ver. Steiermark, 109, 85—95, 2 figs., 5 tab., Graz. FENNINGER, A. & HOLZER, H.-L. (1978): Die Genese der Dolomitsandstein-Folge des Grazer Pa läozoikums. - Mitt. Österr. Geol. Ges., 69, 109-162, 11 figs., 8 tab., 10 pl., Wien. FLAJS, G. (1966): Die Mitteldevon/Oberdevon-Grenze im Paläozoikum von Graz. — N. Jb. Geol. Pa läont. Abh., 124, 221-240, 4 figs., 1 tab., 4 pl., Stuttgart. FLÜGEL, H. (1972): Das Paläozoikum von Graz. - Exk. Führer Tagung Paläont. Ges., 1972, 117- 140, Graz. — (1975): Die Geologie des Grazer Berglandes, 2. Aufl. — Mitt. Abt. Geol. Paläont. Bergb. Landesmus. Joanneum, SH. 1, 288 p., 6 figs., 47 tab., Graz. — & SCHÖNLAUB, H. P. (1970): Nachweis von tieferem Unterdevon und höherem Silur in der Ran nach-Fazies des Grazer Paläozoikums. — Mitt.Geol. Ges. Wien, 63, 142—148, Wien. — & ZIEGLER, W. (1957): Die Gliederung des Oberdevons und Unterkarbons am Steinberg westlich von Graz mit Conodonten. — Mitt. naturwiss. Ver. Steiermark, 87, 25—60, 6 figs., 5 pl., Graz. HERITSCH, F. (1943): Das Paläozoikum. - In: F. HERITSCH & O. KÜHN: Die Stratigraphie der geologischen Formationen der Ostalpen, vol. I, 681 p., Berlin. HÖLLER, H. (1958): Phosphoritknollen im Grazer Paläozoikum. — Mitt.-Bl. Abt. Miner. Landesmus. Joanneum, 1958/1, 35—36, Graz. KHOSROVI-SAID, A. (1962): Stratigraphische Ergebnisse im Paläozoikum beiderseits des Pailgrabens (Graz-N) mit Hilfe von Conodonten. — Anz. Österr. Akad. Wiss. Wien, math.-naturwiss. Kl., 99, 89— 90, Wien. KODSI, M. G. (1967): Zur Kenntnis der Devon/Karbon-Grenze im Paläozoikum von Graz. — N. Jb. Geol. Paläont. Mh., 1967, 415-427, 6 figs., 1 tab., Stuttgart. NÖSSING, L. (1974): Nachweis des tieferen Unterkarbons im Paläozoikum von Graz. — Anz.Österr. Akad. Wiss. Wien, math.-naturwiss. Kl., 1974, 39-41, Wien (1974 a). — (1974): Beitrag zur Kenntnis des Oberdevons und Unterkarbons des Grazer Paläozoikums. — Inaugu ral Diss. Univ. Graz, 103 p., 6 figs., 5 pl., 2 maps, Graz (1974 b). — (1975): Die Sanzenkogel-Schichten (Unterkarbon), eine biostratigraphische Einheit des Grazer Pa läozoikums. — Mitt. naturwiss. Ver. Steiermark, 105, 79—92, 1 fig., 1 tab., 1 pl., Graz. — , EBNER, F. & FLÜGEL, H. W. (1977): Zur Geologie des Eichkogels bei Rein nordwestlich von Graz. — Mitt. naturwiss. Ver. Steiermark, 107, 81—88, 2 figs., 2 tab., Graz. SANDBERG, C. A., ZIEGLER, W., LEUTERITZ, K. & BRILL, S. (1978): Phylogeny, speciation, and 126 zonation of Sivhonodella (Conodonts, Upper Devonian and Lower Carboniferous). — Newsl. Stratigr., 7 (2), 102-120, 2 figs., Berlin/Stuttgart. SANDBERG, C. A. (1979): Devonian and Lower Mississippian Conodont Zonation of the Great Basin and Rocky Mountains. — Brigham Young Univ. Studies Geology, 26, pt. 3, 87—105, 5 figs., Provo. SURENIAN, R. (1977): Biostratigraphie und Sedimentologie der Steinbergkalke (Oberdevon) des Stein berges westlich von Graz. — Inaugural Diss., Univ. Graz, 139 p., Graz. — (1978): Die Conodontenfauna des Steinbergkalkes (Oberdevon, Paläozoikum von Graz). — Mitt. na- turwiss. Ver. Steiermark, 108, 121—135, 4 pl., Graz. UNGER, F. (1843): Geognostische Skizze der Umgebung von Grätz. - In: SCHREINER's „Grätz", 69-82, Graz. WALLISER, O. H. (1964): Conodonten des Silurs. - Abh. hess. L.-Amt Bodenforsch., 41, 106 p., 10 figs., 2 tab., 32 pl., Wiesbaden. 127 Plate 15 Mag. 60 x Carboniferous of Graz Figs. 1—4: Gnathodus sp. A. EBNER 1977; Section Hartbauer, Upper Sanzenkogel Fm., Gnathodus sp. A-Zone. Fig. 5: Gnathodus bilineatus bilineatus (ROUNDY1926); Section Hartbauer, Upper Sanzenkogel Fm., Gnathodus bilineatus bilineatus-Zone. Fig. 6: Gnathodus commutatus mononodosus RHODES, AUSTIN &DRUCE 1969; Section Hartbauer, Gnathodus bilineatus bollandensis-Zone. Fig. 7: Gnathodus commutatus commutatus (BRANSON & MEHL 1941); Section Hartbauer, Upper Sanzenkogel Fm., Upper Gnathodus commutatus nodosus-Zone. Figs. 8, 9: Gnathodus commutatus nodosus BISCHOFF 1957; Section Hartbauer, Upper Sanzenkogel Fm. Fig. 8: Gnathodus bilineatus bollandensis-Zone, fig. 9: Gnathodus commutatus nodosus-Zone. Fig. 10: Gnathodus commutatus multinodosus HIGGINS 1962; Section Hartbauer, Upper Sanzenko gel Fm., Gnathodus bilineatus bollandensis-Zone. Figs. 11, 12: Gnathodus bilineatus bollandensis HIGGINS & BOUCKAERT 1968; Section Hartbauer, Upper Sanzenkogel Fm., Gnathodus bilineatus bollandensis-Zone. Fig. 13: Gnathodus bilineatus bilineatus + Gnathodus bilineatus bollandensis; Section Hartbauer, Up per Sanzenkogel Fm., Gnathodus bilineatus bollandensis-Zone. Figs. 14-18: Declinognathodus noduliferus (ELLISON & GRAVES 1941); Dult Fm., Lower Declino- gnathodus-Idiognathoides-Fauna. Figs. 14, 15, 17, 18: Sanzenkogel, fig. 9: Höchkogel. Figs. 19-21: Declinognathodus lateralis (HIGGINS & BOUCKAERT 1968); Sanzenkogel, Dult Fm., Lower Declinognathodus-Idiognathoides-Fa.una., Figs. 22—24: Gnathodus glaber WIRTH 1967; Gratwein/Au, Dult Fm., Lower Declinognathodus-Idio- gnathoides-Fauna. Figs. 25-29: Idiognathoides convexus (ELLISON & GRAVES 1941); Section Hahngraben, Dult Fm., Lower Declinognathodus-Idiognathoides-Fauna.. Figs. 28, 29 transition forms to Gnathodus glaber WIRTH 1967. Figs. 30-32: Idiognathoides corrugatus (HARRIS & HOLLINGSWORTH 1933); Dult Fm., Lower Declinognathodus-Idiognathoides-Fauna.. Fig. 30: Section NNE Dult Monastery, figs. 31, 32: Section Hahngraben. Fig. 33: Idiognathoides opimus (IGO & KOIKE 1964); Section Hahngraben, Dult Fm., Lower Decli- nognathodus-Idiognathoides-Faxina.. Figs. 34-35: Idiognathoides sinuatus HARRIS & HOLLINGSWORTH 1933;NNEDultMonastery,Dult Fm., Upper Declinognathodus-Idiognathoides-F'auna. Plate 16 Carboniferous (Upper Devonian) of Graz Fig. 1: Siphonodella praesulcata SANDBERG 1972. Steinberg Lst., upper costatus-Zone, Trolp Quar ry (0,66 mm). Fig. 2: Siphonodella praesulcata SANDBERG 1972. Steinberg Lst., upper costatus-Zone, Trolp Quar ry (0,44 mm). Figs. 3, 5: Protognathodus collinsoni ZIEGLER 1969. Steinberg Lst., Protognathodus Fauna, Trolp Quarry (0,76 mm). Figs. 4, 6: Protognathodus kockeli (BISCHOFF 1957). Steinberg Lst., Protognathodus Fauna, Trolp Quarry (0,76 mm). Figs. 7, 8: Gnathodus antetexanus REXROAD & SCOTT 1964. Upper Sanzenkogel Fm., Scaliogna thus anchoralis-Zone, Section Weihermühle (0, 75 mm). Figs. 9, 10: Gnathodus antetexanus REXROAD & SCOTT 1964. Upper Sanzenkogel Fm., Scaliogna thus anchoralis-Zone, Section Hartbauer (0,95 mm). Fig. 11: Gnathodus typicus COOPER 1939. Upper Sanzenkogel Fm., Scaliognathus anchoralis-Zone, Section Hartbauer (1,16 mm). Figs. 12, 13: Gnathodus typicus COOPER 1939. Upper Sanzenkogel Fm., Scaliognathus anchoralis-Zo ne, Section Hartbauer (0,88 mm). Fig. 14: Siphonodella crenulata (COOPER 1939) MT 2 SANDBERG et al. 1978. Upper Sanzenkogel Fm., Scaliognathus anchoralis-Zone, Trolp Quarry (1,02 mm). Figs. 15, 17: Gnathodus texanus ROUNDY 1926. Upper Sanzenkogel Fm., Scaliognathus anchoralis- Zone, Section Weihermühle (1,46 mm). Figs. 16, 18: Gnathodus texanus ROUNDY 1926. Upper Sanzenkogel Fm., Scaliognathus anchoralis- Zone, Section Hartbauer (1,56 mm). Fig. 19: Gnathodus bilineatus bilineatus (ROUNDY 1926). Upper Sanzenkogel Fm., Gnathodus com- mutatus nodosus-Zone, Section Hahngraben (1,2 mm).