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Faciès and biostratigraphy of the Late Carboniferous/Early Permian sedimentary séquence in the Carnic Alps (Austria/ltaly)
Karl KRAINER Institute for Geology and Paleontology, University of Innsbruck,
Innrain 52, A-6020 Innsbruck (Austria)
Karl.Krainer® uibk.ac.at
Vladimir DAVYDOV Department of Geosciences, Boise State University,
1910 University Drive, Boise, Idaho 83725 (USA)
In memoriam Franz Kahler (1900-1996)
KEYWORDS Peri-Tethys,
Late Carboniferous, Early Permian,
Carnic Alps, faciès,
biostratigraphy, fusulinids,
conodonts, plant fossils.
K r a i n e r K. & D a v y d o v V. 1 9 9 8 . — F a c i è s a n d b i o s t r a t i g r a p h y of t he La te Carboniferous/Early Permian sedimentary séquence in the Carnic Alps (Austria/ltaly), in Crasquin-Soleau S., Izart A., Vaslet D. & De Wever P. (eds), Peri-Tethys: stratigraphie cor-relations 2, Geodiversitas 20 (4) : 643-662.
A B S T R A C T
T h e Late Ca tbon i fe tous /Ear ly Permian séquence in the Carn ic Alps
(Austria/ltaly) is a more than 2000 m thick succession of shallow matine
clastic and carbonate sedimentaty rocks. The succession unconformably
overlies rhe folded Variscan basement and is d ivided in to Bombaso
Fo tma t ion , Auernig G r o u p , Rar tendot f G r o u p and Trogkofel G r o u p .
Auernig Group and Rattendorf Group are charactetized by clastic-catbonate
cycles related to Gondwana glacioeustatic sea level changes. Catbonates
contain abundant fossils throughout the séquence, biostratigtaphy is mainly
based on fusulinids. Fine-grained clastic intervais contain abundant plant
fossils, allowing a close corrélation with fluvial succession of the Eastern Alps
(Stangnock Fotmation of the Gutktal Nappe). Fusulinids of the Carnic Alps
show high similarity wirh those of the Russian Platfotm, Donets Basin and
Ptedonets Trough , Southern Urals and particulatly with Central Asia.
Uppermost Moscovian, Kasimovian, Gzhelian, lowermost Asselian, late
Asselian, Sakmarian and Artinskian équivalents ate established and précise
corrélation with sttatotype légions have been completed. Fusulinid, cono-
dont and plant fossil data well coirespond with each othet.
G E O D I V E R S I T A S • 1998 • 2 0 ( 4 ) 643
Krainer K. & Davydov V.
MOTS CLÉS Péri-Téthys,
Carbonifère supérieur, Permien inférieur,
Alpes carniques, faciès,
biostratigraphie, fusulines,
conodontes, plantes fossiles.
R É S U M É
Faciès et biostratigraphie de la séquence sédimentaire Carbonifère supérieur!
Permien inférieur dans les Alpes carniques (Autriche/Italie). La séquence
C a r b o n i f è r e s u p é r i e u r / P e r m i e n in fé r ieur dans les Alpes ca rn iques
(Autriche/Italie) est constituée de plus de 2000 m de roches élastiques et car-
bonatées marines peu profondes. La succession recouvre en discordance le
socle varisque plissé et est subdivisée en la Formation Bombaso, les Groupes
Auernig, Rattendorf et Trogkofel. Les Groupes Auernig et Ratendorf sont
caractérisés par des cycles élastiques et carbonates produits par des variations
glacio-eustatiques (Gondwana). Les carbonates contiennent des fossiles abon
dants tout au long de la séquence, la biostratigraphie étant principalement
fondée sur les fusulines. Les intervalles élastiques fins contiennent des fossiles
de plantes abondants, permettant une corrélation étroite avec la succession
fluviatile des Alpes orientales (Formation Stangnock de la nappe de Gurktal).
Les fusulines des Alpes carniques montrent de grande similarité avec celles de
la plate-forme russe, bassins du Donetz et Predonetz, Oural du Sud et parti
cul ièrement Asie centrale. Des équivalents de la part ie supérieure du
Moscovien, Kasimovien, Gzhélien, de la partie inférieure de l'Assélien, de
l'Assélien supérieur, du Sakmarien et de l'Artinskien ont pu être établis et
une corrélation précise avec les régions stratotypes a été accomplie. Les don
nées sur les fusulines, conodontes et plantes fossiles correspondent bien les
unes aux autres.
I N T R O D U C T I O N
In t he C a r n i c Alps ( sou the rn A u s t r i a / n o r t h e r n
Italy) the folded Variscan basement is unconfor -
mab ly overlain by a th ick succession of shal low
m a r i n e clastic a n d c a r b o n a t e rocks of t he Late
Carboni ferous B o m b a s o Forma t ion and Auern ig
G r o u p a n d t h e Ear ly P e r m i a n R a t t e n d o r f a n d
T r o g k o f e l G r o u p (F ig . 1) . T h è s e r o c k s w e r e
depos i ted in discrète basins formed by b lock and
wrench faulting subséquent to the Variscan o ro
g e n i c p h a s e w i t h i t s c l i m a x d u r i n g t h e
Westphal ian. Classic ou tc rops occur in the cen
tral C a m i c Alps a long the Aust r ian/ I ta l ian border
(Fig. 2 ) . S e d i m e n t a r y rocks o f ail f o r m a t i o n s ,
pa r t i cu l a r l y t h e c a r b o n a t e s , c o n t a i n a b u n d a n t
fossils p r o v i d i n g t h e basis for b i o s t r a t i g r a p h i c
subdiv i s ion a n d cor ré la t ion . B ios t r a t ig raphy of
the Late Paleozoic séquence in the Ca rn ic Alps is
main ly based on fusulinids, a l though p lan t fossils
a n d c o n o d o n t s are of i m p o r t a n c e t o o . D u r i n g
the last décades major progress has been achieved
conce rn ing sedimentology, pa leonto logy and b io
stratigraphy of this séquence (see Flugel 1980 a-b,
1 9 8 1 ; Kahler 1 9 8 3 , 1985 , 1986 , 1989; Fritz et
al. 1 9 9 0 ; Ven tu r in i 1 9 9 0 ; Kra ine r 1 9 9 2 , 1 9 9 3
a n d F o r k e 1 9 9 5 for fu r the r i n f o r m a t i o n s a n d
références). T h e présent paper gives a s u m m a r y
of the Late Carboniferous /Ear ly Permian séquen
ce w i t h spécial emphas i s on the b ios t ra t igraphy
and corrélat ion wi th o ther régions.
FACIES
B O M B A S O F O R M A T I O N
T h e B o m b a s o Fo rma t ion consists of poor ly sort-
ed i m m a t u r e breccias a n d conglomérâ tes wh ich
are e i ther p r e d o m i n a n t l y c o m p o s e d of radiola-
rian cher t and volcanic clasts (Pramollo M e m b e r )
o r o f S i l u r i a n t o D e v o n i a n c a r b o n a t e c las t s
(Mal inf ie r H o r i z o n ) . T h i c k n e s s ranges f rom a
few meters u p to a b o u t 2 0 0 meters . T h e clasts
are der ived from the Variscan b a s e m e n t of the
upl i f ted Pa leoca rn ic C h a i n . T h e success ion of
the B o m b a s o Forma t ion generally shows a fining
upward t rend. Bioclasts of b rach iopods , cr inoids
a n d f u s u l i n i d s a re r a r e l y p r é s e n t i n d i c a t i n g
644 GEODIVERSITAS • 1998 • 2 0 ( 4 )
Waidegger Hbhe 1961
+ Leitenkogel 1845
+
Triassic of the Gartnerkofel-Massif
Rattendorf Group and Trogkofel Group
Bombaso Formation and Auernig Group
ON
FIG. 1. — Map showing the distribution of Late Carboniferous and Early Permian sedimentary rocks in the Carnic Alps (Austria/ltaly).
Krainer K. & Davydov V.
3K
IAN
Goggau L imes tone
(130 m)
_ I
L L Û -z
< AR
TIN
!
T ressdor f L imestone (10 m)
TR
OG
KO
G
RO
U
s
RIA
N
T rogkofe l L imes tone (400 m) T
RO
GK
O
GR
OU
te LU
0.
SA
KM
A
Upper Pseudoschwager ina L imes tone
(Zweikofe l Format ion ; 170 m)
RA
TT
EN
DO
RF
G
RO
UP
A S S E L I A N Grenz land Format ion
(125 m)
RA
TT
EN
DO
RF
G
RO
UP
Lower Pseudoschwager ina L imes tone
(Schul terkofe l Format ion; 160 m) RA
TT
EN
DO
RF
G
RO
UP
tn
o
oc
UJ LL
z
GIA
N Lower Pseudoschwager ina
L imes tone (Schul terkofe l Format ion; 160 m) R
AT
TE
ND
OR
F
GR
OU
P
tn
o
oc
UJ LL
z
OR
EN
BU
R
C a m i z z a Format ion (120 m)
CL
tn
o
oc
UJ LL
z
OR
EN
BU
R
Auern ig Format ion (250 m) R
OU
tn
o
oc
UJ LL
z LIA
N
Co rona Format ion (300 m) M
IG G
O
m
GZ
HE
P izzul Format ion (300 m) U
ER
I
a: K A S I M O V I A N
Meledis Format ion (120 m)
<
o U P P E R M O S T M O S C O V I A N
B o m b a s o F o r m a t i o n
V a r i s c a n B a s e m e n t
FIG. 2 . — S t r a t i g r a p h y o f t h e L a t e C a r b o n i f e r o u s a n d E a r l y
P e r m i a n s t r a t a in t h e C a r n i c A l p s .
déposi t ion in a mar ine env i ronmen t . Thèse bree-
cias a n d cong lomérâ t e s are in t e rp re t ed as mass
gravity flow deposits pr imari ly depos i ted on fan
deltas, part ly subaerially, par t ly submar ine .
A U E R N I G G R O U P
T h e B o m b a s o F o r m a t i o n is o v e r l a i n b y t h e
A u e r n i g G r o u p , w h i c h is u p t o 1.200 m th ick
a n d c o m p o s e d o f M e l e d i s - , P izzu l - , C o r o n a - ,
Auern ig- and Carnizza Format ions according to
Selli (1963) (Fig. 2 ) . T h e succession consists of
cyclic clastic a n d c a r b o n a t e rocks of a sha l low
m a r i n e e n v i r o n m e n t . M e l e d i s - , C o r o n a - a n d
Carn i zza F o r m a t i o n s p r e d o m i n a n t l y consis t of
c l a s t i c s é d i m e n t s , P i z z u l - a n d A u e r n i g
Format ions conta in substant ial quant i t ies of fos-
siliferous ca rbona te rocks. T h e m a i n lithofacies
types are a quar tz - r i ch cong lomera t e of a near-
shore e n v i r o n m e n t , frequently overlain by shale
c o n t a i n i n g a b u n d a n t a n d wel l -preserved mega-
p lan t fossils, t rough-crossbedded a n d h u m m o c k y
c rossbedded s an d s t o n e (shoreface), b i o t u r b a t e d
a n d locally fossiliferous siltstones a n d shales (off
shore) a n d fossi l i ferous l i m e s t o n e s c o n t a i n i n g
c a l c a r e o u s a lgae {Anthracoporella spectabilis,
Archaeolithopbyllum missouriense, Epimastopora,
Eugonophyllum), fusul in ids , small foraminifers ,
e c h i n o d e r m s , b r y o z o a n s , Tubiphytes, s p h i n c t o -
zoans, sol i tary corals a n d o thers . Massive l ime
s tones represen t algal m o u n d s {Anthracoporella
m o u n d s ; K r a i n e r 1 9 9 5 ) , i n t h e M e l e d i s
F o r m a t i o n small m o u n d s f o r m e d of a u l o p o r i d
corals are présen t (Fliigel & Kra iner 1 9 9 2 ) . In
the uppe r par t of the Auern ig G r o u p (Corona- ,
Auern ig- a n d Carnizza Format ions) thèse lithofa
cies t y p e s f o r m p r o m i n e n t c l a s t i c - c a r b o n a t e
regress ive- t ransgress ive cycles ("Auernig cyclo-
themes") w i t h thicknesses of 10-40 m (Fig. 3) .
W i t h i n t h è s e cyc l e s c o n g l o m é r â t e s f o r m e d
d u r i n g relative sea-level lowstands a n d fossilife
rous l imes tone was depos i ted d u r i n g per iods of
relative sea-level h i g h s t a n d s . T h e f o r m a t i o n of
thèse cycles is related to eustatic sea-level changes
c a u s e d by G o n d w a n a n g l a c i a t i o n (Massa r i &
Ventur in i 1990; Krainer 1992 , 1995) .
RATTENDORF G R O U P
T h e Ra t t endo r f G r o u p comprises a succession of
sha l low m a r i n e s é d i m e n t s o f n e a r s h o r e , i n n e r
shelf a n d outer shelf env i ronmen t s . T h e succes
s ion is d iv ided i n t o Lower P s e u d o s c h w a g e r i n a
L i m e s t o n e ( L P L ) , G r e n z l a n d F o r m a t i o n a n d
U p p e r P s e u d o s c h w a g e r i n a L i m e s t o n e ( U P L )
(Fig. 2 ) .
T h e L P L is c o m p o s e d o f t h r e e d e p o s i t i o n a l
cycles cons i s t ing of sha l low m a r i n e l imes tones
and th in intervais of clastic s éd imen t s (Fig. 4 ) .
Clastic intervais form the base of the deposi t io
nal succession a n d were depos i ted du r ing relative
sea-level l o w s t a n d s . D u r i n g t r ansgress ion well
bedded fossiliferous l imestones a n d massive algal
m o u n d s accumula ted . Bedded cher ty l imestones
wi th mar i in te tca la t ions are in te rp re ted to have
been d e p o s i t e d d u r i n g re la t ive sea-level h i g h
stands wi th water dep ths of some tens of meters .
Fusul inid-r ich l imes tone beds are présent in dif
férent s t rat igraphie levels, part icularly at the base
and o n t o p of the clastic intervais. Fusulinids of
thèse beds are cons ide red as p a r a u t o c h t h o n o u s
assemblages, accumula ted du r ing periods of low
646 GEODIVERSITAS • 1998 • 20 (4 )
Late Carboniferous-Early Permian of Carnic Alps
Lithology Faciès
c o n g l o m e r a t e
c o a r s e - g r a i n e d
s a n d s t o n e
f i n e - g r a i n e d
s a n d s t o n e w i t h
h u m m o c k y c r o s s b e d d i n g
s i l t s t o n e ,
b i o t u r b a t i o n
f o s s i l i f e r o u s
b e d d e d l i m e s t o n e
a n d m a s s i v e a l g a l
m o u n d s
Relative Sea-levei
low high
s i l t s t o n e ,
b i o t u r b a t i o n
fine-grained
s a n d s t o n e w i t h
h u m m o c k y c r o s s b e d d i n g
c o a r s e - g r a i n e d
s a n d s t o n e
s h a l e , p l a n t f o s s i l s
c o n g l o m e r a t e
e r o s i v e b a s e
up
per
sh
ore
face
b
each
LST
up
per
sh
ore
face
b
each
low
er
sho
refa
ce
HS
T
c
shel
(o
pen
r> CD
off
sho
i
t -
low
er
sho
refa
ce
.SI
up
per
sh
ore
face
, b
each
up
per
sh
ore
face
, b
each
LST
FIG. 3. — Idealised "Auernig-Cyclothem" from the upper part of the Auernig Group in the Garnitzenberg-Kronalpe area, Carnic Alps.
séd iment i n p u t (see H o m a n n 1969; Flûgel 1974,
1977; Buggisch et al. 1976; Forke et al. in press).
T h e Gtenz land Forma t ion is a cyclic succession,
p r edominan t ly composed of shallow mar ine clas
t ic s é d i m e n t s (quar tz - r i ch c o n g l o m e r a t e , s and
s t o n e a n d s i l t s t o n e ) a n d i n t e t c a l a t e d t h i n
fossiliferous c a r b o n a t e in tervais (Bu t t e r sack &
B o e c k e l m a n n 1 9 8 4 ; B o e c k e l m a n n 1 9 8 5 ) . A
caliche un i t a n d a red shale un i t w i th scattered
angu la r q u a r t z gra ins in t h e u p p e r p a r t of t he
succession indicate subaerial exposure. Fusul inids
were described from rhe th in carbonate inrercala-
t i o n s ( K a h l e r & K a h l e r 1 9 3 7 ; K a h l e r 1 9 8 5 ;
Forke 1995) . P l a n t fossils have been descr ibed
GEODIVERSITAS • 1998 • 20(4) 647
Krainer K. & Davydov V.
f r o m a t h i n s h a l e i n t e r c a l a t i o n b y F r i t z & Boersma (1984) . T h e U p p e r P s e u d o s c h w a g e r i n a L i m e s t o n e is represenred by a cyclic succession composed p te -dominan t ly of dark-grey, th in bedded fossiliferous l imestones and intercalated th in intervais of silt-a n d sands tones a n d fine-grained, w e l l - r o u n d e d a n d w e l l - s o r t e d q u a r t z r i c h c o n g l o m e r a r e s . Limestones contain a b u n d a n t fossils, particularly calcareous algae ( H o m a n n 1972) , small foramini-fers (Fliigel 1971) , fusulinids, corals, bryozoans , brachiopods , gastropods, pelecypods and echino-d e r m fragments. Microfacies has been described by Fliigel (1968) and Buttersack & Boecke lmann ( 1 9 8 4 ) . Cycles ind ica te repeared sh i f t ing f rom nearshore to offshore e n v i r o n m e n t s in an o p e n m a r i n e shelf- lagoon wi th n o r m a l wate r circulat ion (Fliigel 1 9 8 1 ) . C o m p a r e d ro t he L P L a n d Grenzland Format ion the l imestones are characte-rized by more diverse biota a n d microfacies rypes (Fliigel 1 9 7 1 , 1 9 8 1 ; Fliigel et al. 1971) .
TROGKOFEL G R O U P
T h e Trogkofel G r o u p is composed of approx ima-rely 4 0 0 m thick, p r e d o m i n a n t l y massive, subor-dinately bedded l imestones (Trogkofel l imesrone, Tressdorf l imes tone and Goggau l imesrone) . T h e l imestones were depos i ted in shallow, restr icted a n d o p e n m a r i n e s h e l f - l a g o o n s w i t h o n l y m i n o r b a t h y m e t r i c a l d i f f é rences . Tubiphytesl Archaeolithoporella bu i ld -ups c o m p o s e d of sedi-m e n t - b i n d i n g organisms like encrus t ing forami-n i f e r s , p h y l l o i d a l g a e , Tubiphytes, Archaeolithoporella a n d b r y o z o a n s f o r m e d at t he shelf edge (Fliigel 1980a, b , 1981) . Fliigel & Fliigel-Kahler (1980) described 4 6 species of calcareous a l g a e , t h e f u s u l i n i d f a u n a is r e p r e s e n t e d by 70 species (Kahler & Kahler 1980) .
B I O S T R A T I G R A P H Y
FUSULINIDS
T h e first c o m p r e h e n s i v e p a p e r o n f u s u l i n i d s f rom Lare Pa leozo ic l i m e s t o n e s o f t h e C a r n i c Alps was presenred by Schellwien (1898) . F r o m 1 9 3 2 - 1 9 9 6 F. K a h l e r (till 1 9 8 2 w i t h his wife G. Kahler) intensively s tudied the fusulinid fau-
relative sea-level low high
(shoreface) (offshore)
fine-grained sandstones
mariy limestones with mari intercalations
FIG. 4. — Stratigraphie column of the Lower Pseudoschwagerina Limestone (Rattendorf Group) from the north-western side of the Schulterkofel (type section).
n a s o f t h e B o m b a s o F o r m a t i o n , A u e r n i g , Rar t endor f and Trogkofel Groups . T h e biostrat i -graphic classification a n d subdivision of the Late
648 GEODIVERSITAS • 1998 • 20 (4 )
Late Carboniferous-Early Petmian of Carnic Alps
Paleozoic séquence of the Ca rn ic Alps is mainly
based on the detailed investigation of fusulinids
by F. Kahler & G. Kahler. The i r data are publ i -
shed in n u m e r o u s papers , summar ies are given in
Kah le r ( 1 9 8 3 , 1 9 8 5 , 1 9 8 6 , 1 9 8 9 ) . A d d i t i o n a l
data concern ing fusulinid s t ra t igraphy have been
con t r ibu ted by Pasini ( 1 9 6 5 , 1990) a n d recently
by F o r k e ( 1 9 9 5 ) , F o r k e et al. ( in p ress ) a n d
Davydov (Davydov & Krainer, in press). W e use
t he sign * in cases of dif férence f rom or ig ina l
au thors taxonomy.
Bombaso Formation and Meledis Formation
T h e oldest fusulinid fauna of the Ca rn ic Alps is
desc r ibed f rom c a r b o n a t e rocks o n t o p of t h e
Bombaso F o r m a t i o n west of Zollnersee, consis-
t ing of Ozawainella angulata, O. kumpani a n d O.
cf. mosquensis, Fusulinella colaniae rasdorica, F.
fluxa, Beedeina* nytvica callosa, Fusulina (s.str.)
fortissima, Quasifusulinoides* mjachkovensis,
Quasifusulinoides* quasifusulinoides a n d Quasi
fusulinoides juvenatus (Kahler 1983) . Accord ing
to Kah le r ( 1 9 8 3 ) , th is fusu l in id f auna cor res
p o n d s to the Fusulinella bocki zone of the Late
Myachkovian of the Russian classification.
C a r b o n a t e f r o m t h e l o w e r m o s t M e l e d i s
F o r m a t i o n o f t h e A u e r n i g G r o u p y i e l d e d a
Fusulinella, Fusulina a n d Quasifusulinoides fauna
n e a r W a i d e g g e r A l m i n d i c a t i n g l o w e r m o s t
K a s i m o v i a n C 3 A , ( K a h l e r 1 9 8 6 ) a n d a
Protriticites-ïdMna. con ta in ing P. pseudomontiparus
S W o f Z o l l n e r s e e p o i n t i n g t o l o w e r m o s t
Kasimovian A, (Kahler 1983) .
R é c e n t i nves t iga t ion y ie lded a smal l fusu l in id
assemblage from conglomérâtes of the Bombaso
F o r m a t i o n n e a r S t r a n i g e r A l p e , c o m p o s e d o f
Quasifusulinoides quasifusulinoides, Q. fallax,
Q. intermedia, Protriticites ovatus, P. cf. ovoides.
T h e compos i t ion of this assemblage is m o s t simi
l a r t o t h a t f r o m t h e Protriticites ovatus -
Praeobsoletes burkemensis zone in t he s t t a to type
section in the M o s c o w Basin a n d occurs only in
the Peskovskaya Forma t ion of the Myachkovian
H o r i z o n o f t h e M o s c o v i a n ( D a v y d o v 1 9 9 7 ;
Davydov & Krainer, in press). A similar assem
blage was f o u n d near t he t o p of t he B o m b a s o
F o r m a t i o n w e s t o f Z o l l n e r s e e a n d i n c l u d e s
Fusiella lancetiformis, Beedyina consobrina, B. pes-
kensis, B. pseudocylindrica, Fusulinella rara,
Quasifusulinoides pakhrensis, Q. pulchella,
Protriticites ovatus.
C a r b o n a t e s f rom t h e basai Meled i s F o r m a t i o n
n e a r Z o l l n e r s e e a n d a t C i m a Val d i P u a r t i s
conta in fusulinids of the Protriticites pseudomon
tiparus z o n e in its l o w e r m o s t pa r t , a n d of t h e
Montiparus paramontiparus zone in t he m i d d l e
po r t ion of this format ion . T h e Protriticites pseu
domontiparus zone is characterized by Protriticites
globulus, Pr. pseudomontiparus, Pr. sphaericus,
Pr. rotundatus, Pr. ovoides, Pr. lamellosus a n d
Praeobsoletes burkemensis. T h è s e species are cha
racteristic only in the Protriticites pseudomontipa
rus - Obsolètes obsoletus z o n e o f t h e R u s s i a n
P l a t f o r m ( K r e v i a k i a n H o r i z o n ) a n d T i m a n -
P e c h o r a r é g i o n , i n t h e U r a l s , D o n e t s B a s i n ,
Cent ra l Asia, Spitsbergen a n d in the Can tab r i an
M o u n t a i n s (see Davydov & Krainer, in press).
T h e Montiparus paramontiparus subzone is cha
racterized by the occurrence of Praeobsoletes pau-
per, P. burkemensis, Obsolètes timanicus,
O. obsoletus, Montiparus paramontiparus,
M. umbonoplicatus, M. montiparus, M. likharevi,
M. rhombiformis and M. priscus. Montiparus spe
cies f o u n d in t h e C a r n i c Alps are w e l l - k n o w n
from m i d d l e Kas imov ian s t ra ta o f t he Russ ian
P la t fo rm ( K h a m o v n i c h e s k i a n ) , T i m a n - P e c h o r a
Bas in , t h e Ura l s ( u p p e r p a r t o f t h e O r l o v s k y i
H o r i z o n ) , C e n t r a l As ia , S p i t s b e r g e n a n d t h e
Can tab r i an M o u n t a i n s . In Cen t ra l Asia a n d the
Sou the rn Urals the Montiparus montiparus zone
is d ivided in to two subzones: the M. paramonti
parus subzone in the lower par t a n d the M. sub-
crassulus s u b z o n e i n t h e u p p e r p a r t . T h e
assemblage recognized in the Ca rn ic Alps corres
p o n d s to the M. paramontiparus subzone (see dis
cussion by Davydov & Krainer) .
It should be indica ted tha t the représentatives of
the Praeobsoletes-Obsoletes l ineage in the C a r n i c
Alps appear later. In t he Russian P la t form, the
Ura ls , D o n e t s Basin a n d C e n t r a l Asia Praeob
soletes first a p p e a r s in t h e u p p e r m o s t M y a c h
k o v i a n a n d r a n g e s i n t o t h e l o w e r m o s t Kas i
movian . Obsolètes first appears at the base of the
K a s i m o v i a n a n d is m o s t cha rac t e r i s t i c for t h e
E a r l y K a s i m o v i a n ( K r e v i a k i a n ) . O n l y r a r e ly
Obsolètes r a n g e s i n t o t h e m i d d l e K a s i m o v i a n
(Kahmovn ichesk ian ) . In t he C a r n i c Alps , s imi-
l a r l y w i t h t h e C a n t a b r i a n M o u n t a i n s a n d
GEODIVERSITAS • 1998 • 20 (4 ) 649
Krainer K. & Davydov V.
S p i t s b e r g e n ( V i l l a et al. 1 9 9 2 ; N i l s s o n &
D a v y d o v 1 9 9 3 ) , t h e r e p r é s e n t a t i v e s o f t h e
Praeobsoletes-Obsoletes l i n e a g e a r e r a r e .
Praeobsoletes first appears only in the lowermost
K a s i m o v i a n ( K r e v i a k i a n ) a n d Obsolètes f i rs t
appears in the u p p e r m o s t Kreviakian or only in
the Khamovnichesk ian .
In the very rop of the Meledis Fo rma t ion in rhe
R C section ( R C - 1 2 b a n d R C - 1 3 ) the following
fusulinids we te ident i f ied: Ferganites ferganensis
Miklukha -Mac lay , Rauserites sp. , a n d Rauserites
rossicus (Schellwien) (Fig. 5A-E) . T h e last species
in the Russian Platform a n d the Urals characteri-
se lowermost Gzhel ian or Rechitskyi H o r i z o n of
t h e R u s s i a n P l a t f o r m ( R o s o v s k a y a 1 9 5 8 ;
Makh l ina et al. 1984; Davydov & Popov 1986) .
Ferganites ferganensis in Cent ra l Asia as well as in
S. U r a l s cha rac t e r i s e s also ear ly G z h e l i a n , an
équivalent of Amerevskyi H o r i z o n of the Russian
P l a t f o r m (F ig . 6) ( D a v y d o v & P o p o v 1 9 8 6 ;
P o p o v et al. 1 9 8 9 ) . W e sugges t t h a t t h e very
upper po r t i on of the Meledis Fo rma t ion is early
Gzhel ian in âge (Fig. 6) .
Pizzul Formation, Corona Formation, Auernig
Formation and Carnizza Formation
A c c o r d i n g t o K a h l e t ( 1 9 8 5 ) t h e P i z z u l
Formar ion (Untere kalkreiche Schichrgruppe) is
characterized by the occurrence of the following
fusulinid species: Triticites oryziformis, Rauserites*
noinskyi plicatus; Daixina alpina vetusta,
D. sokensis (s.srr.*), D. naviculaeformis, D. sakma-
rensis a n d Quasifusulina eleganta. Récent studies
of n o n - o r i e n t e d t h i n - s e c t i o n s f rom rhe Pizzul
Fo rma t ion show d o m i n a n c e of a Schagonella and
Daixina fauna. Because in Cent ra l Asia a n d sou
thern Urals représentatives of the Daixina soken
sis g r o u p a p p e a r ea r l i e r t h a n i n t h e R u s s i a n
Platform, a n d because of the s t ra t igraphie posi
t i o n o f t h e P izzu l F o t m a t i o n a b o v e t h e ear ly
Gzhel ian a n d below the O r e n b u r g i a n , we believe
tha t the Pizzul Fo rma t ion has to be an équivalent
of the late Gzhel ian (s.str.).
F r o m a t h i n c a r b o n a t e b e d o f t h e C o r o n a
F o r m a t i o n at Ga rn i t zenbe rg (Mit t lere ka lka rme
S c h i c h t g r u p p e ) K a h l e r ( 1 9 8 3 ) r e p o r t e d
"Pseudofusulina multiseptata". Daixina alpina, D.
ex gr. admirabilis a n d Schagonella spp . also were
r e c e n t l y i d e n t i f i e d b y D a v y d o v . T h e spec ie s
Pseudofusulina multisepta o r i g i n a r e d f rom the
C a r n i c A lps (Sche l lwien 1 8 9 8 ) , b u t for m o r e
t h e n sixty years was used in t he l i t e ra ture as a
Late Permian Parafusulina species, reporred from
m a n y Tethyan régions. Unt i l revision and solving
of rhis t a x o n o m i c a l p r o b l e m s we use i nve r t ed
c o m m a s for this species.
In Darvas and in S. Urals Schagonella in gênerai
d o m i n a t e d in t h e m i d d l e G z h e l i a n . Daixina
admirabilis o r ig ina l ly was d e s c r i b e d f rom t h e
O r e n b u r g i a n of the Urals (Zolotova et al. 1978) ,
b u t a lso was r e p o r t e d f rom t h e la te G z h e l i a n
(s.str.) of Darvas (Davydov 1986) . Fusul in id data
f t o m P i z z u l a n d C o r o n a F o r m a t i o n s d o n o t
cons t ra in a spécifie âge. Based o n the strarigra-
ph ic posir ion of Pizzul and C o r o n a Format ions
above an équivalent of the early Gzhel ian (Upper
Meled is ) a n d be low t h e O r e n b u r g i a n A u e r n i g
F o r m a r i o n , t he âge of b o t h fo rmar ions can be
e s t i m a t e d as late G z h e l i a n (s.str.) (Amerevskyi
a n d P a v l o v o p o s a d s k y i H o r i z o n s o f R u s s i a n
Platform).
T h e A u e r n i g F o r m a r i o n ( O b è r e k a l k r e i c h e
Sch ich tg ruppe) of G a r n i t z e n b e r g a n d Krona lpe
conta ins Boultonia europaea; Triticites schivageri-
niformis, T. perstabilis; Daixina*alpina, D.*com-
munis, D. * alpina fragilis, D. * devexa acallosa;
"Pseudofusulina multiseptata", "P. paraconcinna";
Dutkevitchia dastarensis, D. "kargalensis", D. "ruz-
hencevi"; Quasifusulina tenuissima, Q. compacta,
Q. karawankensis, Q. kaspiensis, Q. phaselus,
Q. pseudoelongata, Q. pseudolonga (Kahler 1983 ,
1985) .
T h e C a r n i z z a F o r m a t i o n ( O b è r e k a l k a r m e
S c h i c h r g r u p p e ) o f G a r n i t z e n b e r g c o n t a i n s
Daixina alpina antiqua = alpina and the subspe-
cies fragilis, a n d Dutkevitchia dastarensis.
A c c o r d i n g t o K a h l e r ( 1 9 8 6 , 1 9 8 9 ) P i z z u l
F o r m a r i o n , C o r o n a F o r m a r i o n , A u e r n i g
F o r m a t i o n a n d C a r n i z z a F o r m a t i o n a r e o f
Gzhel ian âge (Gzhel ian E).
R é c e n t s t ud i e s in t h e s o u t h e r n Ura l s , D o n e t s
Basin a n d in Cent ra l Asia (Darvas and sou the rn
Fe rgana ) s h o w e d t h a t Boultonia europaea a n d
Dutkevitchia dastarensis first appear at the basai
O t e n b u r g i a n Daixina sokensis z o n e ( D a v y d o v
1984 , 1992 ; Popov et al. 1989 ; Davydov et al.
1993) . Dutkevitchia ruzhenzevi a n d Dutkevitchia
kargalensis eve rywhere first a p p e a r on ly in t he
650 GEODIVERSITAS • 1998 • 20 (4 )
Late Carboniferous-Early Permian of Carnic Alps
FIG. 5. — Stratigraphically significant fusulinids from the Meledis Formation (basai Auernig Group) and Lower Pseudoschwagerina Limestone (Rattendorf Group). k,Rauserites rossicus (Schellwien, 1908), tangential section, RC-13-4. B , Rausehtes sp., oblique section, RC-13-4. C - E , Ferganites aff. ferganensis (Miklukho-Maclay, 1948): C , axial section, RC-12b-9; D , tangential section, RC-12b-12; E, paraxial section, RC-12b-2. F , G , Schellwienia bornemani (Leven ef Scherbovich, 1978): F, axial section of typical spécimen, SK-157-4; G , axial section of short spécimen, SK-157-2. H , Zigarella panjiensis (Leven ef Scherbovich, 1978), axial section of typical spécimen, SK-157-5. I, Likharevites inglorius (Bensh, 1962), axial section, SK-157-1. J - L , Schellwienia bornemani (Leven ef Scherbovich, 1978): J , axial section of spécimen with small axial fillings, SK-157-12; K, axial section of typical spécimen, SK-157-13; L , axial section of short spécimen, SK-157-9. Scale bar: 0,5 cm.
GEODIVERSITAS • 1998 • 20 (4 ) 651
Krainer K. & Davydov V.
early Asselian, a n d we believe t h a t their occur
rence in the O r e n b u r g i a n Auern ig Forma t ion is
misidentif ied. Therefore we place inverted c o m -
m a s w i t h b o t h o f t h è s e s p e c i e s . T h e âge o f
Auern ig and Carnizza Format ions for n o w can be
e s t i m a t e d as O r e n b u r g i a n ( é q u i v a l e n t o f
N o g o n s k i a n of Russian Platform) (Fig. 6) .
Lower Pseudoschwagerina Limestone (Schulterkofel
Formation)
F r o m t h e u p p e r m o s t p a r t o f t h e L o w e r
Pseudoschwager ina L i m e s t o n e near R u d n i g a l m
Kahler (1985) described the following fusulinid
species: Boultonia europaea; Rugosofusulina aria-
nica, R. directa, R. latioralis, R. cf. pandae,
R. praevia egregia, R. stabilis, R. stabilis longa;
Paraschwagerina cf. tinvenkiangi elongata,
Occidentoschwagerina alpina a n d "Eozellia miha-
ranoensis" (= Ultradaixina ex gr. postgallowayi).
F r o m S c h u l t e t k o f e l K a h l e r ( 1 9 8 3 ) l i s t e d
Boultonia europaea; Ruzhenzevites* parasolidus;
Rugosofusulina cf. pandae, R. serrata, R. likana,
R. praevia a n d Rugosochusenella*pseudogregaria.
In a récent paper Kahler & Krainer (1993) des
c r i b e d a f u s u l i n i d f a u n a c o m p o s e d o f a b o u t
30 species from the upper par t of the LPL of the
Schu l te rkofe l s ec t ion . Species o f Triticites a n d
Rugosofusulina d o m i n a t e , whereas those of rare
"Daixina" {^Schellwienia), Rugosochusenella a n d
Ruzhenzevites occur. T h e Carbon i fe rous /Permian
b o u n d a r y was d r a w n at t he first appea rance of
"Pseudoschwagerina" a n d "Occidentoschwagerina
alpina" {- Ultradaixina) in the uppe r par t of the
s e c t i o n . F t o m o u r p o i n t o f v i ew, s p é c i m e n s
n a m e d as Pseudoschwagerina could no t be ident i -
fied even wi th genus n a m e , because in the tan
g e n t i a l s e c t i o n s r e p o r t e d , t h e j u v e n a r i u m
s t ruc ture , w h i c h is m o s t i m p o r t a n t for t axono -
my, is n o t présent.
Accord ing to Forke et al. (in press) the lower par t
( d e p o s i t i o n a l S é q u e n c e 1) o f t h e L P L in t h e
Schulterkofel section, characterized by the occur
r e n c e o f Ruzhenzevites ferganensis a n d
Ruzhenzevites parasolidus w i t h o u t species of the
g e n u s Ultradaixina, is c o r r e l a t e d w i t h t h e
Sokensis z o n e . T h e ove r ly ing p a r t ( u p p e r m o s t
par t of deposi t ional Séquence 1 u p to the t o p of
d e p o s i t i o n a l S é q u e n c e 3) c o r r e s p o n d s t o t h e
Bosbytauensis-Robusta zone . T h e C / P - b o u n d a r y
of Forke et al. lies near the base of the overlying
Grenz land Format ion .
T h e fol lowing species were ident i f ied in récent
s tudies of LPL in t he Schul terkofe l sec t ion: in
t h e v e r y l o w e r p o r t i o n o f L P L ( T S T o f
S é q u e n c e 1) w e f o u n d Daixina sokensis,
Schellwienia oblonga a n d Dutkevitchia bimorpha.
In the H S T of Séquence 1 Ultradaixina postso-
kensis a n d Schellwienia ulukensis a n d w i t h i n
Séquence 2 , Schellwienia ulukensis a n d Zigarella
elegans w e r e i den t i f i ed . M o s t i n t e r e s t i n g d a t a
were retrieved from the t o p of Séquence 3 , where
Schwagerina versabile, Schellwienia bornemani,
Zigarella panjiensis a n d Likharevites inglorius were
identified (Fig. 5 F-L).
To est imate the âge of the LPL Forma t ion we can
indicate the following: in Sou the rn Fergana a n d
Darvas Ruzhenzevites ferganensis first appea ts in
t h e m i d d l e p o r t i o n o f a n é q u i v a l e n t o f t h e
Daixina sokensis zone. (Davydov 1984; Popov et
al. 1 9 8 9 ) . Ruzhenzevites parasolidus is a m o r e
advanced species a n d in Darvas it first appears in
t he very t o p of t h e Daixina sokensis z o n e a n d
r a n g e s h i g h e r . I n S o u t h e r n a n d N o r t h e r n
Fergana this species occurs in t he Schwagerina
robusta-Ultradaixina bosbytauensis z o n e a n d
tanges higher in to the Asselian. Schellwienia ulu
kensis in Cent ra l Asia as well as in the Sou the rn
Ura l s s e c t i o n o c c u r s o n l y in t h e Schwagerina
robusta-Ultradaixina bosbytauensis z o n e .
Schwagerina versabile in D a t v a s a n d i n t h e
S o u t h e r n Urals appears in t h e very t o p o f t he
Schwagerina robusta-Ultradaixina bosbytauensis
zone, b u t is character is t ic of the early Asselian.
Schellwienia bornemani, Zigarella panjiensis a n d
Likharevites inglorius in C e n t r a l Asia a n d t h e
Sou the rn Urals are k n o w n only from the Asselian
( B e n s h 1 9 6 2 ; L e v e n & S c h e r b o v i c h 1 9 7 8 ;
Davydov 1984; Popov et al. 1989) (see corréla
t ion char t , Fig. 6) .
Based o n ail this da ta we can suggest the follo
w i n g . T h e T S T ( t r a n s g r e s s i v e Sys tems t r a c t ;
Fig. 4) of Séquence 1 of LPL can be correlated
wi th the u p p e r m o s t par t of the Daixina sokensis
z o n e . T h e H S T ( h i g h s t a n d Sys tems t r a c t ) o f
Séquence 1 can be correlated wi th the lower por
t ion of the Schwagerina robusta-Ultradaixina bos
bytauensis z o n e o r w i t h t h e Ultradaixina
postsokensis z o n e o f t h e S o u t h e r n U r a l s a n d
652 GEODIVERSITAS • 1998 • 20 (4 )
Late Carboniferous-Early Permian of Carnic Alps
D a r v a s . M o s r p a r t of S é q u e n c e 2 (excepr t h e H S T ) convent ional ly can be correlated wi th the m i d d l e p o r t i o n o f t h e Schwagerina robusta-Ultradaixina bosbytauensis z o n e o r w i t h t h e Ultradaixina bosbytauensis zone of the S o u t h e t n Urals and Darvas . T h e H S T of Séquence 2 a n d L S T ( l o w s t a n d S y s t e m s t r a c t ) a n d T S T o f Séquence 3 should be correlared wirh the upper por t ion of the Schwagerina robusta-Ultradaixina bosbytauensis zone or wi th rhe Ultradaixina post-gallowayi zone of the Sou the rn Urals a n d Darvas . T h e H S T of Séquence 3 very probably is Early Asselian in âge. T h e lasr conclus ion is based on rhe following: in Darvas , the Sou thern Urals a n d in the D o n e t s Basin the acme-zone ( m a x i m u m of occurrences) fot Ultradaixina is in the upper port i o n ( b u t n o t u p p e r m o s t ) o f t he Schwagerina robusta-Ultradaixina bosbytauensis zone . In t he very uppe r p o r t i o n of this zone Ultradaixina is rare a n d pe thaps extinct, and absolutely absent in the Asselian. Similarly in the Schulterkofel sect ion the a c m e - z o n e for t he Ultradaixina is the H S T of Séquence 2 and the L S T of Séquence 3 . In the T S T of Séquence 3 Ultradaixina is extre-mely rare a n d absolutely no Ultradaixina is présen t in t h e H S T of S é q u e n c e 3 . Schellwienia bornemani and Zigarella panjiensis originally were described from the midd le Asselian of Darvas . In r h e S o u t h e t n U r a l s t h e y o c c u r in t h e ea r ly -midd le Asselian. Likharevites inglorius in Darvas , N o r t h e r n F e r g a n a , t h e S o u t h e r n U r a l s a n d Predoners Trough was found in the ear ly-middle Asse l ian ( B e n s h 1 9 6 2 ; Leven & S c h e r b o v i c h 1978; Davydov 1990; Davydov et al. 1993) . So, occurrences of Schellwienia bornemani, Zigarella panjiensis a n d Likharevites inglorius s u g g e s t Asselian âge for the H S T of Séquence 3 of the Lower Pseudoschwagerina Limestone .
Grenzland Formation F t o m l imestones of the Grenz land Forma t ion at Rudnigsa t te l Kahler (1985) repor ted the occurrence of Quasifusulina cf. compacta, Q. eleganta, Q. kaspiensis, "Darvasites contractus", Zigarella
pseudopointeli, Sphaeroschwagerina carniolica, Pseudoschwagerina extensa a n d Sphaeroschwagerina sphaerica. F r o m the type sec t ion near R a t t e n d o r f e r A l m , Kahler & Kahler (1937) described Pseudoschwa
gerina aequalis, Ps. extensa a n d Sphaeroschwagerina* confinii, f r o m t h e e a s t e r n s i d e o f S c h u l t e r k o f e l , Pseudoschwagerina turbida a n d Sphaeroschwagerina * carniolica. Based o n the o c c u r r e n c e of Pseudoschwagerina aequalis, Sphaeroschwagerina* confinii a n d Sphaeroschwagerina* carniolica K a h l e r ( 1 9 8 6 ) d a t e d t h e G r e n z l a n d F o r m a r i o n as m i d d l e Asselian.
Forke (1995) descr ibed Sphaeroschwagerina glo-merosa f r o m t h e G r e n z l a n d F o r m a t i o n n e a r Rudnigsat te l . M o s t of t h e species of G r e n z l a n d F o r m a t i o n , except Quasifusulina species, are k n o w n from the m i d d l e as w e l l as f r o m t h e l a t e A s s e l i a n . Sphaeroschwagerina glomerosa indicates on ly late Asselian âge. Base on this we can suggest midd le -late Assel ian âge for the G r e n z l a n d F o r m a t i o n (see Fig. 6) .
Upper Pseudoschwagerina Limestone F r o m t h e t y p e s e c t i o n o f t h e U p p e r P s e u d o s c h w a g e r i n a L i m e s t o n e at Z o t t a c h k o p f Kahler described the following fusulinid species: Boultonia willsi, Pseudofusulina regularis, McCloudia* haydeni, Darvasites contractus, Schwagerina "krtowf, Pseudoschwagerina pulchra, Biwaella inopinata a n d Rugosochusenella paragre-garia. Red l imestones at T t o g h ô h e a n d at p o i n t 2 0 1 6 (according to Kahler be longing to the Trogkofel L i m e s r o n e , a f t e r F o r k e t o t h e U p p e r P s e u d o s c h w a g e r i n a L i m e s t o n e ) c o n t a i n a r ich fusul in id fauna. Kahler ( 1 9 8 3 , 1985) r e p o r t e d t h e f o l l o w i n g s p e c i e s : Boultonia willsi, Quasifusulina nimia, Q. pseudoelongata, Q. tenuissima, Q. cf. kaspiensis, " Chusenella cheni", "Ch. chihsiaensis", "Ch. rabatei", Schwagerina* moelleri, Schw.*paraconfusa, Eoparafusulina* " tschernyschewi', Robustoschwagerina geyeri, R. schellwieni, Paraschwagerina inflata longa, Sphaeroschwagerina * carniolica, S. * lata, S. * pulchra, Zellia heritschi, Z. galatea. A c c o r d i n g to Fo rke ( 1 9 9 5 ) t h e red l imes tones con ta in the following stratigraphically i m p o r t a n t s p e c i e s : Zellia heritschi, Robustoschwagerina schellwieni, R. geyeri, Paraschwagerina inflata, Schwagerina moelleri, Schwagerina cf. verneuili
GEODIVERSITAS • 1998 • 20 (4 ) 653
Krainer K. & Davydov V.
FIG. 6. — Corrélation chart for the Late Carboniferous and Early Permian.
654 GEODIVERSITAS • 1998 • 20
Late Carboniferous-Early Permian of Carnic
GEODIVERSITAS • 1998 • 20 (4 )
Krainer K. & Davydov V.
a n d Pseudofusulinoid.es pusillus. F o r k e ( 1 9 9 5 )
dates rhe U p p e r Pseudoschwager ina Limesrone as
Sakmar i an (Robustoschwagerina geyeri zone a n d
Zellia heritschi zone) .
Trogkofel Group
Af te r K a h l e r & K a h l e r ( 1 9 8 0 ) t h e f u s u l i n i d
fauna of the Trogkofel G r o u p consisrs ma in ly of
species of the gênera Triticites, Darvasites, Pseudo-
fusulinoides, Pseudofusulina, " Praeparafusulina",
Pamirina a n d Minojapanella. T h e y d e s c r i b e d
a b o u t seventy species. S t ra t ig raphica l ly i m p o r
tan t index fossils are Schwagerina* moelleri, cha-
r a c t e r i s t i c f o r t h e l o w e r p a r t ( T r o g k o f e l
l imesrone) , "Parafusulina lutuginf typical for the
T r e s s d o r f l i m e s t o n e , a n d t h e Chalaroschwa-
gerina* vulgaris-gtoup t o g e t h e t w i t h Pamirina
darvasica in the Goggau l imestone . True parafu-
sulinids a n d Misellina species are lacking.
Kahler (1986) da ted the Trogkofel l imes tone as
Sakmarian (Tastubian-Ster l i tamakian) due to the
occurrence of Robustoschwagerina schellwieni and
Pseudoschwagerina lata. T h e Tressdorf l imestone,
c o n t a i n i n g "Praeparafusulina lutugini" is classi-
f ied as E a r l y A r t i n s k i a n ( B u r c h e v ) , a n d t h e
G o g g a u l i m e s t o n e , w h i c h c o n t a i n s Chalaro-
schwagerina* vulgaris a n d Pamirina, is da ted as
L a t e A t t i n s k i a n ( I r g i n ) . A c c o r d i n g t o F o r k e
( 1 9 9 5 ) t h e T r o g k o f e l l i m e s t o n e is L a t e
Sakmar ian to Eatly At t insk ian in âge.
I t s h o u l d b e n o t e d , t h a t S a k m a r i a n a n d
Ar t insk ian fusulinids of the Urals can no t occur
in t h e T e t h y a n s e c t i o n , as t h e C a r n i c A l p s ,
because b e g i n n i n g in t he ear ly S a k m a r i a n t h e
Boréal province was comple te ly isolated from the
T e t h y a n p rov inces . N o n e A r t i n s k i a n fusu l in id
species of the Urals are k n o w n from Tethys sédi
men t s , b u t those listed, we believe, are identified
e r roneous ly . For th i s r eason "Praeparafusulina
lutugini" takes i nve r t ed c o m m a s a n d ind ica tes
taxonomical misidentif icat ion.
W e c a n n o t e s t i m a t e t h e âge o f t h e Trogkofe l
l imesrone based on ly o n fusul inids for now. It
could be Sakmat i an as well as early Ar t insk ian .
B e c a u s e t h e G o g g a u L i m e s t o n e c o n t a i n s
Chalaroschwagerina vulgaris a n d Pamirina darva
sica, w h i c h in D a r v a s c h a r a c t e r i s e s t h e l a t e
Y a k h t a s h i a n (Ea r ly A r t i n s k i a n ) ( L e v e n et al.
1992) , we can convent ional ly es t imate the âge of
t h e T r e s s d o r f l i m e s t o n e as e a r l y A r t i n s k i a n
(Fig. 6) .
T h e fol lowing p rob l ems for fusul inid biosrrari-
graphy shou ld be addressed immedia te ly :
- p r éc i s e f u s u l i n i d b i o s t r a t i g r a p h y o f P izzu l ,
Corona , Auern ig a n d Carnizza Format ions ;
- complè te charactet ist ic of C / P b o u n d a r y beds
a n d be t t e r cr i ter ia for t he C / P b o u n d a r y pos i
t ion;
- âge of Grenz land Format ion ;
- fusulinid biost ra t igraphy a n d succession of the
Trogkofel Limestone;
- r e s tudy of t he Tres sdor f a n d G o g g a u L i m e
stones.
CONODONTS
T h e occur rence of c o n o d o n t s in Late Paleozoic
carbonates of the Ca rn ic Alps was first n o t ed by
Fliigel et al. (1971) from the Ra t t endo r f G r o u p
a n d B o e c k e l m a n n ( 1 9 8 3 ) f r o m t h e A u e r n i g
G r o u p (discoveries of individual c o n o d o n r frag
ments , wh ich have n o s t ra t igtaphic impor tance ) .
Forke (1995) descr ibed a c o n o d o n t fauna from
red l imestones of the U p p e r Pseudoschwager ina
Limesrone. T h e c o n o d o n t fauna is c o m p o s e d of
t h e f o l l o w i n g s p e c i e s : Aethotaxis advena,
Hindeodus minutus, Mesogondolella cf. bisselli,
Diplognathodus expansus?, Sweetognathus inorna-
tus a n d Sweetognathus aff. whitei.
In c e n t r a l a n d w e s t e r n U S A S. inornatus a n d
S. aff. whitei appea r in t he Late W o l f c a m p i a n .
S. inornatus belongs to the Sweetognathus whitei-
Mesogondolella bisselli z o n e . I n t h e U t a l s ,
Sweetognathus inornatus a p p e a r s i n t h e
Ster l i tamakian (Late Sakmarian) a n d ranges in to
the A t t i n s k i a n . Sweetognathus whitei is k n o w n
only in Aktastian (Early Artinskian) (Chernykh &
R e s h e t k o v a 1 9 8 7 ; C h e r n y k h & C h u v a s h o v
1 9 9 3 ) . Sweetognathus whitei in t h e Trogkofe l
G r o u p is represented by incomplè te atypical spé
c i m e n s ( i den r i f i ed w i t h "af f in i ty" s i g n ) . T h e
appearance of Sweetognathus inornatus and S. aff.
whitei t o g e t h e r w i t h Robustoschwagerina a n d
Zellia, b u t w i t h o u t typical A t t in sk ian fusul inid
faunas (Pamirina, Chalaroschwagerina) in t h e
Carnic Alps, indicates at this t ime Sakmarian âge.
A c c o r d i n g to Forke (1995) the U p p e t P s e u d o
s c h w a g e r i n a L i m e s r o n e is o f S a k m a r i a n âge
656 GEODIVERSITAS • 1998 • 20 (4 )
Late Carboniferotis-Early Permian of Catnic Alps
(based o n the occurrence of Robustoschwagerina
geyeri a n d Zellia heritschî). Forke (1995) in his
p a p e r p r é s e n t s c o r r é l a t i o n c h a r t s o f t h e
R a t t e n d o r f a n d Trogkofel G r o u p w i t h sect ions
f r o m t h e U r a l s , D a r v a s , N - C h i n a , S - C h i n a ,
Japan and USA.
FOSSIL FLORA
Plan t fossils were r e p o r t e d f rom the B o m b a s o
F o r m a t i o n a n d A u e r n i g G r o u p m o r e t h a n
100 years ago. Hôfer seems to be the first w h o
c o l l e c t e d p l a n t fossils in 1 8 6 9 in t h e M o n t e
C o r o n a / K r o n a l p e and Casera Fo r /Ofena lm area.
T h e spéc imens were d e t e r m i n e d a n d descr ibed
by U n g e r ( 1 8 6 9 ) , t h e t a p h o f l o r a list c o n t a i n s
19 taxa.
T h e dé te rmina t ions of Unger (1869) were later
r e v i s e d b y R e i c h a r d t ( 1 9 3 7 ) a n d F r i t z &
Boersma (1982) .
Taphoflora lists from the M o n t e C o r o n a section
( C o r o n a F o r m a t i o n ) have b e e n p u b l i s h e d by
Stache (1874) , Schellwien (1892) , Frech (1894)
and Geyer (1897) .
F r o m t h e local i t ies C a s o n d i Lanza (?Meledis
Format ion) a n d M o n t e Pizzul (type locality for
the Pizzul Fo rma t ion ) p lan t fossils were descri
b e d by T o m m a s i ( 1 8 8 9 ) , Bozz i ( 1 8 9 0 ) a n d
Vinassa D e Regny & Gor t an i (1905) .
Later, n u m e r o u s n e w locali t ies of p l a n t fossils
w i t h i n t he A u e r n i g G r o u p were d iscovered by
Kahler, Me tz a n d others in the Auernig , Nassfeld
a n d Schul terkofe l areas. T h e p l a n t fossils were
descr ibed by Re i cha rd t ( 1 9 3 3 ) a n d Kie lhauser
(1937) , a first s u m m a r y on the fossil flora of the
Auern ig G r o u p inc lud ing 25 taxa was given by
Reichardt (1937) a n d j o n g m a n s (1938) .
J o n g m a n s ( 1 9 3 8 ) c l a s s i f i ed t h e f lo ra o f t h e
A u e r n i g G r o u p as W e s t p h a l i a n D (= E a r l y
S t e p h a n i a n ) a n d W e s t p h a l i a n E (= L a t e
S tephanian) . H e also po in ted ou t tha t w i th in the
Auernig G r o u p the Schulterkofel flora represents
the youngest flora.
Berger ( i 9 6 0 ) repor ted 30 taxa from n e w locali
t i e s , m o s t o f t h e m w i t h i n t h e B o m b a s o
F o r m a t i o n a n d l o w e r m o s t p a r t of t he A u e r n i g
G r o u p . H e c l a s s i f i e d t h e foss i l f l o r a as
Westphal ian D . Plant fossils have also been des
c r i b e d f rom several n e w in t e rva i s w i t h i n t h e
u p p e r m o s t C o r o n a - , A u e r n i g - a n d C a r n i z z a
Format ions . (Kahler et al. 1933 ; Kahler & Prey
1963 ; Fenninger & Schon laub 1972; Francavilla
1974) .
F r i t z & B o e r s m a ( s i n c e 1 9 8 0 ) a n d F r i t z &
Krainer (since 1993) systematically invest igated
the fossil flora of the B o m b a s o F o r m a t i o n a n d
A u e r n i g G r o u p f rom m o r e t h a n 3 0 local i t ies .
P lan t fossils are f o u n d in ail fo rma t ions of the
Auern ig G r o u p , f rom mos t localities t he strat i
g r a p h i e p o s i t i o n w i t h i n t he s e c t i o n is exac t ly
k n o w n .
F r o m ai l l o c a l i t i e s 1 0 5 t a x a a r e d e s c r i b e d
( E q u i s e t o p h y t a 2 6 t a x a , L y c o p h y t a 12 t a x a ,
F i l i cophyta , P t e r i d o s p e r m a e a n d P t e r i d o p h y l l a
5 7 t axa , C o r d a i t o s p e r m a e 9 t axa ; C o n i f e r a e
1 t axon , see Fri tz et al. 1 9 9 0 ; F t i tz & Kra iner
1993 , 1994, 1995) .
F r o m the G t e n z l a n d F o r m a t i o n t he occur rence
of p l a n t fossils ( n o d é t e r m i n a t i o n s ) has b e e n
n o t e d by severa l a u t h o r s (Felser et al. 1 9 5 6 ;
Felser & K a h l e r 1 9 6 3 ; K a h l e r & Prey 1 9 6 3 ;
Flùgel 197A). He rzog (1984) discovered a p lan t
fossil bear ing interval and collected a flora which
w a s d e t e r m i n e d a n d d e s c r i b e d b y F r i t z &
Boersma (1984) a n d Fritz et al. ( 1 9 9 0 ) . So far
k n o w n this local i ty is t he on ly o n e w i t h i n t he
R a t t e n d o r f G r o u p a n d thus the younges t fossil
flora of the Late Paleozoic séquence in the Carn ic
Alps.
FLORA OF T H E B O M B A S O F O R M A T I O N
From the Bombaso Format ion 3 localities conta i
n ing p lan t fossils are k n o w n (Tomri tsch 1, 2 a n d
6) . T h e lowermost locality (Tomri tsch 6) is cha-
racter ized by t he occu r r ence of Sphenophyllum
oblongifolium, Linopteris neuropteroid.es,
Neuropteris ovata, Neuropteris scheuchzeri a n d
o t h e r s (Fr i tz & K r a i n e r 1 9 9 5 ) . A c c o r d i n g t o
Wagner (1984) N. scheuchzeri is a guideform of
the C a n t a b r i a n {Odontopteris cantabrica zone ) .
T h i s corrélat ion qui te precisely corresponds wi th
fusu l in id d a t a , w h i c h sugges ts for C a n t a b r i a n
U p p e r m o s t Moscovian a n d Early Kasimovian âge
( G i n k e l 1 9 7 1 ; R a u s e r - C h e r n o u s o v a &
Scherbovich 1974) .
FLORA OF T H E AUERNIG G R O U P
From the Auern ig G r o u p p lan t fossils are k n o w n
from m a n y hor izons wi th in ail format ions . T h e
GEODIVERSITAS • 1998 • 20 (4 ) 657
Krainer K. & Davydov V.
l o w e r m o s t h o r i z o n c o n t a i n i n g p l a n t fossils is f r o m p e r h a p s t h e b a s a i p a r t o f t h e M e l e d i s F o r m a t i o n ( local i t ies T o m r i t s c h 3 , Z o l l n e r s e e a n d S t ran ige r A l m ) . T h e fossil assemblages of rhese localiries are characterized by the a b u n d a n -ce o f Linopteris neuropteroid.es. T h e présence of Sphenophyllum angustifolium, S. oblongifolium, Callipteridium pteridium, Odontopteris brardii a n d Pecopteris species of the g r o u p P. arborescence -P. schlotheimii indicates S tephan ian âge (early to midd le S tephan ian C according to the megaflora zona t ion of W a g n e r 1984) . However , there is a cont rad ic t ion berween fusulinid a n d floral da t ing of the lower Meledis Fo rma t ion . Based on fusulin i d s t h e lower M e l e d i s F o r m a t i o n is Ear ly to M i d d l e K a s i m o v i a n in âge a n d s h o u l d cor res p o n d a t l eas t w i t h t h e u p p e r p o r t i o n o f t h e C a n t a b r i a n , S t e p h a n i a n A a n d p e r h a p s S t ephan ian B (Wagner & W i n k l e r - P r i n s 1 9 8 5 ; D a v y d o v 1 9 9 0 ) . O n l y rhe u p p e r m o s r Me led i s Formar ion , wh ich conta ins early Gzhel ian fusulinids , could cor respond wi th S tephanian C . T h e âge of the Meledis Format ion in the Tomri tsch 3, Zo l lne r see a n d S t ran iger A l m localiries s h o u l d also be dated by fusulinids.
T h e u p p e r m o s t p o r t i o n of the A u e t n i g G t o u p con ta in ing p lan t fossils lies w i th in the u p p e t par t o f t h e C a r n i z z a F o r m a t i o n ( l o c a l i t y S c h u l t e r k o f e l ) . F r o m t h i s l o c a l i t y F r i t z & Boersma ( 1 9 8 1 , 1983) Fritz et al. (1990) described a flora composed of 30 taxa, characterized by the occurrence of Callipteridium gigas, C. pteridium, Odontopteris alpina, O. brardii, Pecopteris feminaeformis a n d i n d e x f o s s i l s f o r L a t e Srephanian âge: Aphlebia elongata, Pseudomario-pteris busquetii a n d Sphenophyllum alatifolium [Sphenophyllum angustifolium zone, Stephanian C according to W a g n e r 1984) .
FLORA OF T H E G R E N Z L A N D F O R M A T I O N
T h e flora of the Grenz land F o r m a t i o n conta ins 16 species inc lud ing Annularia sphenophylloides, A. stellata, Sphenophyllum cf. angustifolium, Callipteris conferta, Odontopteris brardii, Pecopteris feminaeformis and P. schlotheimii. T h e o c c u r r e n c e o f Callipteris conferta a n d Sphenophyllum cf. angustifolium indicates Early Permian â g e {Callipteris conferta z o n e a c c o r d i n g to W a g n e r 1984) .
Typical guideforms of the Lobatopteris lamuriana z o n e (Bar rue l ian) a n d Alethopteris zeilleri zone ( S t e p h a n i a n B) h a v e n o t b e e n d i s c o v e r e d till now. A c c o r d i n g to t h e p l a n t fossi ls t h e B o m b a s o F o r m a t i o n is o f C a n t a b t i a n âge , t h e A u e r n i g G r o u p conta ins rypical guideforms of Srephanian C , a n d rhe Grenz land Forma t ion is characterized by a flora of Early Permian âge (see Table Ca rn ic Alps, this vo lume) . Based o n D o n e t s Basin data ( D a v y d o v 1990) S t e p h a n i a n A c o r r e s p o n d s to the midd le and perhaps par t of late Kasimovian, S tephanian B cor responds to the late Kasimovian a n d S tephanian C to the mos t parr of Gzhel ian . A u r u n i a n begins from the Schwagerina robusta-Ultradaixina bosbytauensis z o n e o f t h e O r e n b u r g i a n a n d also co t responds to the whole Asselian (Fig. 6) .
T h e flora of rhe B o m b a s o F o r m a t i o n , A u e t n i g G r o u p , a n d Grenz l and Formar ion is well dared by fusul inids . Fluvial séquences of t he Eas t e tn Alps ( S t a n g n o c k F o r m a t i o n , G u t k t a l N a p p e ) , wh ich conta in a similar assemblage of p lan t fossils r a n g i n g f fom rhe Odontopteris cantabrica zone ro the Callipteris conferta zone , can be well c o r r e l a t e d w i t h t h e m a r i n e s é q u e n c e o f t h e C a i n i c A l p s ( B o m b a s o F o t m a t i o n - G r e n z l a n d Forma t ion ) .
Acknowledgements K. K. wishes to t h a n k the Austr ian Academy of S c i e n c e s ( C o m m i s s i o n for S t r a r i g r a p h y ) for f inanc ia l s u p p o r t of field w o r k in rhe C a r n i c Alps . B o t h a u t h o t s t h a n k D o r a Gal legos from B o i s e S t a t e U n i v e r s i t y for c o r r e c t i o n o f t h e English. T h e Permian Research Ins t i tu te at Boise State Univers i ty p rov ided s u p p o r t for th in -sec -t ion prépara t ion a n d s tudy of fusulinid biostrat ig r a p h y . W e a re v e r y g r a t e f u l t o A l a i n I z a r t (Nancy) a n d Danie l Vachard (Lille) for reviewing rhe m a n u s c r i p r a n d m a k i n g helpful c o m m e n t s and suggestions.
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Submitted for publication on 1 January 1997; accepted on 15 December 1997.
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