Records of the Western Australian MuseulIl Supplement No. 58: 305-319 (2000).
Late Devonian-Early Carboniferous transgressions and regressions
in the Camic Alps (Italy)
Maria Cristina Perri and Claudia Spalletta
Dipartimento di Scienze della Terra e Geologico-Ambientali, University of Bologna, Italy
Abstract
Sediments deposited from the Frasnian (Late Devonian) to the
Bashkirian (Late Carboniferous) in the Carnic Alps represent a regional
transgressive sequence documenting Frasnian drowning of the Middle
Devonian-Iower Frasnian reefs, overlap by micritic oozes, and followed by
radiolarian chert and siliciclastic turbidites. The micritic Iithostratigraphic
interval deposited during upper Frasnian-Iower Visean has been investigated
by qualitative and quantitative analysis of conodont associations.
Study of 36 stratigraphic sections, ranging from the Upper rhenana Zone
(Frasnian) to salldbergi Zone (Tournaisian), enabled application of existing
models of conodont biofacies relating the conodont-genera associations to
depositional environments (Sandberg 1976; Sandberg and Ziegler 1979;
Sandberg and Dreesen 1984; Ziegler and Sandberg 1984). Changes in
biofacies, from deep to less deep, may indicate regressive trends even in
monotonous micritic lithofacies. Preliminary data resulting from the biofacies
analysis of 365 samples are presented.
The local transgression-regression curve inferred from the data has been
compared with the T-R Devonian sea-level curve for Euramerica (Johnson et
al 1985; Sandberg et al. 1988; Johnson and Sandberg 1989) and with the
Carboniferous eustatic curve (Ross and Ross 1988). The lower part of the
Carnic Alps sea-level curve from Middle triangularis to the Uppermost
margillifera Zone displays a tectonically-driven transgressive trend. Only in
the Upper rhomboidea Zone does an eustatic regressive event appear to be
partly identifiable. In the upper part of the local sea-level curve, from the
Lower traehytera to the salldbergi Zones, the transgressive-regressive events
correspond to eustatic ones. The only exception is a tectonically-driven local
regressive event during the Lower expallsa Zone. The global Middle
praesulcata-Upper praesuleata zones regression is evident and, as in other
European areas, it extends to the sulcata Zone (Bless 1993; Bless et al. 1993) in
contrast with the global transgression at the base of the Carboniferous.
INTRODUCTION
An Upper Devonian-Lower Carboniferous
limestone sequence extends throughout the
Carnic Alps. The succession, deposited from
Frasnian to lower Visean, is characterized by a
monotonous micritic facies rich in ammonoids
and other pelagic fossils. The corresponding
lithostratigraphic unit, the clymenid and
goniatitid limestone, has been investigated by
means of conodont associations to define a
detailed biostratigraphy. This has provided
more precise information on ages than was
previously known. Intensive sampling for
conodonts in the Italian
area of the
unit
p
upper Frasnian-midd
ian data for conodont biofac cs
As conodonts appear to be distributed
according to depth rather than other limiting
factors, changes in biofacies may reflect eustatic
and/ or tectonic sea level changes which would
be difficult, if not impossible, to detect by other
means of geological analysis in a monotonous
micritic sequence.
The same unit has already undergone biofacies
analysis in two sections cropping out in Austria at
the Cresta Verde and at Kronofgraben (Dreesen
1992). The resulting data reflect the regression in
Euramerica at the Devonian-Carboniferous
boundary.
The present investigation was designed to probe
the following questions:
1) If change of depth can be demonstrated by
conodont biofacies analysis, even in a micritic
sequence.
2) If conodont biofacies analysis can be used to
recognise transgression-regression (T-R) events
in a similar kind of succession.
3) If comparison between global and local sealevel curves can make it possible to discriminate
records of global T-R events from tectonicallydriven local T-R events.
306
M.C. Perri, C. Spalletta
STRATIGRAPHY AND LITHOLOGIES
In the Carnic Alps a regional transgressive
sequence accumulated from the Frasnian (Upper
Devonian) to the Bashkirian (Upper Carboniferous).
This transgressive trend is documented by the
Frasnian drowning of the Eifelian (Middle
Devonian)-lower Frasnian reefs, overlap by micrite
oozes, and subsequent accumulation of radiolarian
chert and siliciclastic turbidites of the Hochwipfel
Formation (middle Visean-Bashkirian). The micritic
deposition began during the Frasnian when
synsedimentary extensional faults broke up the
reefs and inaugurated conditions of deeper
sedimentation. The synsedimentary extensional
tectonics is indicated by slumping, turbiditic layers
(Perri and Spalletta 1990; Spalletta, Perri and
Pondrelli 1998a) and breccias (Perri and Spalletta
1981; Spalletta et al. 1983; Spalletta and Perri 1998a);
these occur up to the end of the Uppermost
marginifera Zone (mid-Famennian) (Kreutzer 1990).
Very thin scattered calcarenite to calcilutite layers,
interpreted as distal turbidites (Perri and Spalletta
1998a), and/or contourites (Spalletta and Perri
'::-.
1994) are found up to the top of the unit. Neptunian
dykes are present in the upper part of the carbonate
sequence primarily near the contact with the
overlying Hochwipfel Formation (Perri and
Spalletta 1998a).
The micritic deposits constitute an informal
lithostratigraphic unit, the clymenid and goniatitid
limestone, deposited from upper Frasnian to lower
Visean (Early Carboniferous). The carbonate unit
corresponds to the 'Calcari a Climenie' described
by Gortani (1907). This historical name was recently
rejected by Venturini and Spalletta (1998) on the
basis of stratigraphical range since the clymenids
died out at the end of the Upper Devonian. Basing
their observations solely on palaeontological
content, Austrian authors (e.g. Schonlaub 1985;
Schonlaub et al. 1988) subdivide the unit into Pal
Limestone for the Upper Devonian part, and Kronof
Limestone for the Lower Carboniferous. Venturini
and Spalletta (1998), however, taking into account
the homogeneity of the unit and rare occurrence of
well preserved ammonoids in outcrops, prefer to
consider it as a single unit. The whole unit is
MOOSKOfEL
"
ARVENIS M
"
) .Bema
f
Fwitzer,aOd
(l,/
• Milano
~ T~rino
I~
Genova
Figure 1
Map showing location of examined sections.
Devonian-Carboniferous T-R pattern in the Carnic Alps
307
characterized by variability of thickness, ranging
from a minimum of about 80 m to a maximum of
about 200 m. It consists of grey, light pink to
reddish micrite with beds 0.5-3cm thick. The
original layers, planar to slightly wavy bedded, are
usually overprinted with stylolites, and with
occasional ochreous marly to shaly interbeds a few
mm in thickness.
The microfacies consists of biomicrite, for the
most part wackestone, but also packstone and
mudstone; in thin sections the rock often appears
recrystallized. The fossil content consists mainly of
pelagic fossils such as dymenids, goniatites,
trilobites and radiolarians. Brachiopods,
orthoceratids, ostracodes and crinoids columnals
are also found. Goniatites and clymenids are most
commonly found from the upper Famennian part of
the unit (from the Lower expansa Zone). The
samples produced a highly variable number of
conodonts and even some vertebrate microremains.
have been recognized (Perri and Spalletta 1990, 1991,
1998b-f; Perri et al. 1998; Spalletta and Perri 1998a-b;
Spalletta et al. 1998b).
This work constitutes a preliminary synthesis of
conodont biofacies analysis carried out on 36
stratigraphic sections ranging from the Upper
rhenana Zone (upper Frasnian) to the sandbergi Zone
(middle Tournaisian). The conodont biofacies
models proposed for this time period (Sandberg
1976; Sandberg and Ziegler 1979; Sandberg and
Dreesen 1984; Ziegler and Sandberg 1984) associate
genera with depositional environments. The
conodont biofacies analysis was conducted
applying the rules for recognizing biofacies
proposed by Ziegler and Sandberg (1990).
The sections, all characterized by a monotonous
micritic lithology, crop out on the Italian side of the
Camic Alps from Mt. Coglians to Mt. bstemig,
mainly in the area of Monte Croce Carnico Pass
(Figures 1-4). The 365 samples analyzed yielded
just under 58,000 Pa elements, all identified and
counted. Samples with less than 10 Pa elements
were considered statistically insignificant. Biofacies
analysis was then carried out for each of the
remaining 320 samples, section by section. Data
arising from this analysis has been summarized and
the number of samples assigned to each biofacies,
and reported by biozone (Figure 5). Figures 5, 6, 7
report the transgressive and regressive events
CONODONT BIOFACIES
Quantitative and qualitative study of conodont
associations of the clymenid and goniatitid limestones
in a large number of upper Frasnian-Iower Visean
sections produced enough data to begin the process of
conodont biofacies analysis. Twenty-three of the 28
conodont biozones discriminated in this time interval
Figure 2
Location map of the sections: 1) Wolayer Glacier (WG); 2) Canalone Collina Est (CCLE); Casera Collinetta di
Sopra (CCS); Sentiero per Cresta Verde (SCV); Sentiero Storico A (SSA); Sentiero Storico C (SSC); Sentiero
Storico D (SSD); Casera Collinetta di Sotto A (CSA); Casera Collinetta di Sotto C (CSC); Casera Collinetta di
Sotto B (CSB); Passo di Monte Croce Carnico (pMC); Cava Val Grande (CVG); Val Grande (VG); Cava
Cantoniera (CC).
M.C. Perri, C. Spalletta
308
Figure 3
Location map of the sections: 3) Trincea A (TRA); Trincea
(TR); Oleodotto (aLE); Pal Grande (PG); Rio Grande
(RG); 4) Pizzo Timau A (PTA); Lago A (LGA); Lago C
(LGC); Pramosio A (PRA); Rio Boreado (RB); Pramosio
(PR); Pramosio Bassa (PB); Malpasso A (MLA); Malpasso
(ML); Malpasso C (MLC); Malpasso B (MLB).
Figure 4
Location map of the sections: 5) Lodin (LD);
Cercevesa (CRC); Chiarso (CHR); Las Callas
(LC); Plan di Zermula C (PZC); 6) Ostemig (OS).
Devonian-Carboniferous T-R pattern in the Carnic Alps
pa pa-po pO
sandbergi
T
U. duplicata
T
6
2
L duplicata
T
slllcata
R
4
U. praesulcata
R
3
M. praeslllcata
Rff
L praesulcata
T
10
U. expansa
M. expansa
T
14
T
9
2
L expansa
T
24
39
U. postera
R
5
7
L postera
Rff
3
15
2
U. trachytera
T
31
6
L trachytera
T
7
5
Us!. marginifera
R
16
U. marginifera
U. marginifera
R
24
1
T
16
3
L marginifera
U. rhomboidea
TIR
6
I
R
10
10
L rhomboidea
Us!. crepida
R
11
3
T
2
U. crepida
T
M. crepida
L crepida
Tff
T
U. triangularis
M. triangularis
T
3
TIR
2
L triangularis
R
Iinguiformis
U. rhenana
mIX.
2
RffIR
2
Rff
5
309
The samples have been referred to three biofacies:
palmatolepid (pa), palmatolepid-polygnathid (papo) and polygnathid (po), in order from deep to
less deep environments. The palmatolepid biofacies
is substituted by the palmatolepid-bispathodid (pabi) biofacies in the second half of the Famennian
(from the Lower expansa Zone) when species
belonging to BispatllOdus Muller become abundant
and by the siphonodellid biofacies in the lower
Tournaisian (from the sulcata Zone) (Ziegler and
Sandberg 1990) when Siphonodella Branson and
Mehl completely supplants its ecologic equivalent
Palmatolepis Ulrich and Bassler (Ziegler and
Sandberg 1984). The palmatolepid biofacies is
inferred to denote continental rise and lower slope
environments; palmatolepid-polygnathid biofacies
to imply middle and upper slope, and polygnathid
biofacies to denote outer shelf (Sandberg and
Dreesen 1984). Some samples were assigned to
mixed biofacies. The palmatolepid or palmatolepidbispathodid biofacies is the most prevalent biofacies
(Figure 6). The palmatolepid-polygnathid biofacies
is the second most widely represented; it is
sometimes equivalent to the pa biofacies, as in the
Upper rhomboidea Zone, or even predominates, as in
the Lower postera, Upper postera and Lower expansa
zones. The polygnathid biofacies occurs only three
times: in the Upper rhenana, Lower postera-Upper
postera and Upper praesulcata-sulcata zones. Mixed
biofacies are present in the Middle triangularis,
Upper crepida-Uppermost crepida and Lower
rllOmboidea zones.
2
DETAILED ANALYSIS (Figure 7)
Figure 5
Number of samples assigned to each biofacies
per biozone, pa: palmatolepid biofacies (or
palmatolepid-bispathodid or siphonodellid);
pa-po: palmatolepid-polygnathid biofacies;
po: polygnathid biofacies; mix.: mixed
biofacies. The transgressive and regressive
events described for Euramerica are reported
in a column to the right of the conodont
biozone. The regression in the slllcata Zone IS
Inferred by European data and the
transgression of the
Zone from
European and northeastern Australia data.
described for Euramerica (]ohnson et al. 1985;
Sandberg et al. 1988; Johnson and Sandberg 1989) in
a column aligned with the conodont biozones. Some
biozones can be seen to be characterized
an
transgnosslve and
eustatic
analysis for the
ra Zone demonstrates that samples
assigned to the lower part of the biozone can be
discriminated from those referred to the upper part
of the biozone. In the other cases such
discrimination has not been possible.
Upper rhenana-linguifonnis Zone
The few samples referred to this interval are
characterized by the predominance of the
palmatolepid-polygnathid (pa-po) biofacies,
although the polygnathid (po) biofacies also occurs
in the Lower rhenana Zone. No sample was assigned
to the palmatolepid (pa) biofacies even though the
Carnic basin was deepening during this time
interval. The samples thus reflect the Upper
rhenana-linguiformis Zone regression reported for
Euramerica. Further studies, including the Lower
triangularis Zone are in progress.
Middle triangularis-Uppermost crepida Zone
The interval from the upper part of the Middle
triangularis Zone to the Uppermost crepida Zone is
characterized in Euramerica by a transgressive
Irend. The data confirm a transgressive trend
connected with continued drowning of the basin
during this interval. The pa biofacies is
predominant but mixed biofacies also occur,
probably a result of transport connected with
synsedimentary extensional tectonic activity.
310
M.C. Perri, C. Spalletta
.pa
El pa-po
Gpo
o mixed
:l
i
~
Figure 6
S ~
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C.
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..J
u
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Diagram with the number of samples assigned to each biofacies per biozone. Pa biofacies predominates, papo is the second widely represented biofacies and po biofacies occurs three times. Mixed biofacies are
present in the lower part of the diagram. Biofacies abbreviations and T-R events as in Figure 5.
U, duplicata T
L dupll;;ara T
1--------------1
sulcala R
u
e
~
g
8- ~
e
~
~
t:
f-
rr~suk<da
M praesukata
R
Rrr
1--------------1
M eJtpansa T
L C'Jlpansa T
U po-slera R
Lower rhomboidea-Uppennost marginifera Zone
Two regressive events occurred in Euramerica
during this interval. The first is recorded from the
Lower rhomboidea Zone up to the first part of the
Lower marginfera Zone, and the second from the
upper part of the Upper marginifera to the
Uppermost marginifera Zone. The pa biofacies is
predominant in the studied sections. The
tectonically driven local transgressive trend masks
the Euramerican regressive events. The effects of
the global regressive event and of the local
transgressive trend offset each other during the
Upper rhomboidea Zone.
L. poslera RIf
Lower trachytera-Upper trachytera Zone
Predominance of the pa biofacies during this
interval is in accord with the local transgressive
trend documented for Euramerica.
U trachylC'ra T
USI
margioikra R
U, margioifera R
Lower postera-Upper postera Zone
The pa-po biofacies predominates, with some
occurrences of the po biofacies. The change in
biofacies clearly accords with the record of
regression in Euramerica.
L marginikra TIR
U, rhomboidea R
1.. dwmboidea R
USI crepida T
U, crepida T
M acrida
Trr
L crepida T
M mangutaris: T/R
L rnangularis R
Imguit{jnm~
R!T/R
Li, rhenana RfT
0
3
~
Figure 7
0
-g
III
~
•
~
Diagram reporting the data of the last two
previous figures as percentages. The changes
of biofacies per biozone are clearly readable.
Biofacies abbreviations and T-R events as in
Figure 5.
Lower expansa-Lower praesulcata Zone
The interval is characterized by an important
transgressive event in Euramerica. There is
evidence of the expansa Zone transgression also in
northeastern Australia (Talent 1989; Mawson and
Talent 1997) and in northwest Africa (Wendt and
Belka 1991). In the examined sections the
palmatolepid-bispathodid biofacies is widespread.
The only exception is for the Lower expansa Zone
where the less deep pa-po biofacies prevails,
continuing the regressive trend of the postera Zone.
In contrast with the global transgressive trend and
with comprehensive geologic data indicating a
general transgressive trend for the Carnic basin
Devonian-Carboniferous T-R pattern in the Carnic Alps
311
from Frasnian to Bashkirian, the presence of this
biofacies may indicate a tectonically-driven local
regression of minor order. This regression could be
related to uplift of some fault-bounded blocks, as
proposed by Spalletta and Venturini (1988, 1994) to
explain deposition of part of the Hochwipfel
Formation, and the sedimentary interval at the top
of the limestone succession during a major
transgressive cycle in the Camic basin. Uplift of
tectonic blocks could be explained by strike-slip
tectonics regulating basin evolution (Vai 1991) for
the entire Palaeozoic circum-Mediterranean area.
ecologic equivalent of the pa biofacies. It is taken to
be evidence of a transgressive event already
reported for other European areas (Bless 1993; Bless
et al. 1993), and for northeastem Australia as well
(Talent 1989; Mawson and Talent 1997).
In support of the above, a selection of the more
significant sections with their conodont
biostratigraphic data and biofacies analysis are
presented. The data corroborate regression in the
postera Zone continuing in the Camic Alps into the
Lower expansa Zone, regression in the Upper
praesulcata Zone extending into the sulcata Zone,
and transgression in the Middle and Upper expansa
Zone and the sandbergi Zone.
Four sections, Casera Collinetta di Sotto B (CSB),
Casera Collinetta di Sotto A (CSA), Sentiero Storico
A (SSA) and Sentiero per Cresta Verde (SCV),
outcrop in the Monte Croce Camico Pass area
(Figure 2). A fifth section, Plan di Zermula C (PZe),
crops out in the Mt. Zermula area (Figure 4).
Biostratigraphic analysis of the CSB and CSA
sections is reported in Perri and Spalletta (1998c and
1998e).
Section CSB ranges from the Upper marginifera
Zone to the Upper postera Zone (Figure 8). In this
section the very high percentage of Palmatolepis
tends to decrease in the postera Zone with the
concomitant increase of Polygnathus. In the first part
of the section, up to sample CSB21, predominance
of the pa biofacies is apparent changing to a pa-po
Upper praesulcata-sulcata Zone
The global regression, reported for Euramerica
and northwest Africa (Wendt and Belka 1991)
during the Middle praesulcata-Upper praesulcata
Zone, is indicated by the exclusive occurrence of po
biofacies. This biofacies continued to prevail during
the sulcata Zone as already reported by Dreesen
(1992) and supported by the present data. The
regressive trend thus persisted in the Camic Alps
as in other European areas (Bless 1993; Bless et al.
1993), in contrast with the global transgression at
the base of the Carboniferous (Ross and Ross 1988).
sandbergi Zone
During the biozone the predominant
siphonodellid biofacies, defined by the high
percentage of Siphonodella, is considered to be an
Casel'J ColllneHd Ul SOIlO B (('58)
('SRI CS82 ('S8' CSB4 (,SE!.' CSBt> ('S87 ('SBx CSSY CSBln ('S811 ('S81? CSBI\ ('S81" CSB1A ('SBIl) C'S8?1 C'S8?? CSB?' ('S8?4 ('S8?"
15)\
\0
.AI
B,
B,
4.'
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IO,n
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x.,
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Of',!
.Mc
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Figure 8
Percentage distribution of conodont genera in the Casera Collinetta di Sotto B (CSB) section. Numerical
values, biozonal and biofacies assignments and computer generated diagram. AI: AItemognathlls, Bi:
Bispathodlls; Br: Bramrzehla; Me: Mehlina; Pa: Palmatolepis; Po: Polygnathlls; Se: Scaphignatlllls.
312
M.C. Perri, C. Spalletta
Casera Collinelta di Sotto A (CSA)
CSAI CSA2 CSA3 CSA4 CSA5 CSM CSA) CSA8 CSM CSAIIl CSAII CSAI2 CSAI3A CSAI3
AI
9.1
19J)
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Hr
27.3
37.7
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9.5
2f1,O
HI
0.9
0.8
"le"
Mc
Pa
Po
Ps
Si
54.5
54.7
3Jl
1.9
6.1
1.9
66.7
4.8
.59.5
2A
4.8
1.7
1.8
0.9
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19.0
lA
B.1l
37.5
0.4
0.7
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9.6
5.2
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10.2
67.8
56,6
43.5
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Cascra Collinelta di S<JHo A (CSA)
OSi
OP,
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OPa
.Mc
l!I"le"
.Hr
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l1li AI
O!J(
;;:
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Figure 9
N
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u
:<
u
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;;,"
u
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"'
u
~
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N
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;;;
u
~
u
-<
'"
u
-<
"'
u
Percentage distribution of conodont genera in the Casera Collinetta di Sotto A (CSA) section. Numerical
values, biozonal and biofacies assignments and computer generated diagram. AI: Alterrzognathus; Bi:
Bispathodus; Br: Branmehla; "le": "Icriodus"; Me: Mehlina; Pa: Palmatolepis; Po: Polygnathus; Ps:
Pseudopolygnathus; Si: Siphonodella.
biofacies (Figure 8). Change of the predominant
biofacies from deep (pa) to less deep (pa-po)
accords with the global postera Zone regression.
Among samples referred to the postera Zone, only
three - CSB27, CSB29 and CSB30 - have been
assigned to the pa biofacies. This assignment was
based on the high percentage of the Branmehla,
whose proportion, however, fluctuates widely
through the section. This extreme variability in the
percentage of Branmehla is common in all
Famennian sections in the Carnic Alps.
Section CSA ranges from the Upper trachytera
Zone to the Lower praesulcata Zone (Figure 9). The
lower portion of the section (CSAI-CSA5), referred
to the Upper trachytera Zone, has been assigned to
the pa biofacies because of the high percentage of
Palmatolepis and Branmehla. During this interval the
percentage of Polygnathus is very low. From sample
CSA6 to CSA12, referred to the Lower posteraLower expansa Zone, the high percentage of
Palmatolepis tends to decrease. On the other hand,
the percentage of Polygnathus increases sharply
allowing the assignment of this part of the section
to the less deep pa-po biofacies; it accords with the
global record of regression in the postera Zone. In
the Carnic Alps this continued during the Lower
expansa Zone.
The upper part of the section, from sample
CSA13A to CSA13C is referred to the top of the
Lower expansa Zone up to the Lower praesulcata
Zone and is characterized by a high percentage of
Palmatolepis and Bispathodus and a low percentage
of Polygnathus. Thus, this portion of the section can
be assigned to the deeper pa-bi biofacies; this is in
keeping with the global transgression reported for
Euramerica, northeastern Australia and northwest
Africa.
Section SSA ranges from the Lower expansa to the
Lower praesulcata Zone (Figures 10 A-B). The
percentage of Palmatolepis remains almost constant.
In contrast, the percentages of Polygnathus and
Bispathodus are changeable. The values for
Polygnathus are high in the first half of the section
(SSA2-SSA7) decreasing in the upper part, whereas
the percentage of Bispathodus increases greatly in
the second half (SSA8-SSA14). The data allow this
Devonian-Carboniferous T-R pattern in the Carnic Alps
313
A
Senliero Slorico A (SSA)
Weight (g)
2855
264D
2325
t1'is.Jli'i
P,
II
sp
P,
p,
19
grac. gracilis
I
2830
261 )
14
57
9
83
42
9
13
16
21
I
222
21
167
Pa. per!. !tChindcwolfi
P,
p,
PI. conditus
Pb
I
8 Pa
9
P,
p,
6
Pa grac.
~lgtnQidahs
Po. s.emicostarus
~Mt.~
Po. "P
Po. granulosus
Si. stabilis MJ
I
7
I
I
6
Me. ';.trigo<.a
P,
p,
I
23
Pa. perlobaLa maxima
P,
I
I
Po. slyriacu'i
p,
38
Br wemeri
P,
P,
5
P,
p,
35
183
218
I
8
9
Br. bohlcnana
Pa. rugoS<! ampla
Po. pr3ehassi
Po. marginvoluluS
Po. s.emicostatus
Ps. brevipennatus
BI. stabilisMI
2
70
Ih,1
2( J.{ ~
2, I
4,0
9,5
8.5
7
17
119
10
2
15
26
7
P.
S
5
Hi. bispathodus
p.
S
Si. jugosus
P.
14
Br. inomata
P.
I
Bi. aculea«u!i
4
Bi. costa«us M2
P.
Pa
Pa
Bi. ultimus M2
Pa
4
4
P.
Si. pn~esulcata
P,
Pa
P.
Bi, costatus
Po. inomalus
Total
3
14
8
10
8
27
4
I)
12
4
19
5
Senll('rn StmlCo A (SSA)
18
39
2
5
.1
4
I
566
!Ot'JC;'
I
i-
61
174
HOq
h(l0(
OP,
95
94
92
OPo
4(Jof
OPa
.Me
.Br
200/('
.Br
35
33
19
125
lA
44
J3
89
7,2
S
19
9
15
13,7
14
I
7
15
tt,x
:B
8
Pa
Pa. grac. ellpans.a
lA
t'i,\
14.9
2
57
5
28
Pa. grac. gonyoclimeniae Pa
Br. suprema
I.X
U
1.1
3
P.
Figure 10
no
18
Po. znepolensis
P,
29.0
,1.:U 29){ YHl
5.'1,.\
1,6
1.6
2h, I
I
Po. extralobatus
Pa
P,
\.1
p,
I
Bi. uJtimu~ Ml
.;L6
Pll
1.1
q.7
.'i4,,\
2
12
I
Ps. marb. trigonicus
\.\
38
P.
P.
P.
Po. corn. communis
41.1
1.1
27.4
4D
Bi. coslatus M I
"\h,1
n.9
36
Bi. sr.abilis M2
liA
2fjJl
4 1.0
'J Pa
Pa. rugosa
11.1
41.5
4
Po. obliquicostarus
I ]J
2X,6
14A
2
3
Pa. rugosa rugos.a
Br
I
I
8
14
SSA2 SSA) SSA5 SSA6 SSt\"7 SSAX SSt\9 SS!\ 10 SSA 12 SSA 11 SSA \·1
HI
Me
Pa 15.7 1\,.\
9
Pa. perlobara postent
~Mt
38
Pa
Pa
p,
Branmehla s-p. A
Po. ;;cmicostatus
24
I
P,
p,
p,
p,
Ps. micropunctatus
Sentiero Storico A (SSA)
69
5
P,
p,
Pa. grac. manea
B
18
93
W'*
N
<:
~
~ <
~
'"
<:
uo
uo
<
uo
uo
'"uo<:
Vi
'" -<: :::<:
<:
uo
uo
~
~
::::;
:':
~
Vi
<:
uo
I
69 I4DI
Numerical values, biozonal and biofacies assignments and computer generated diagram. A Numerical
distribution of conodont taxa in the Sentiero Storico A (SSA) section. Bi: BispatllOdus; Br: Branmehla; Me:
Mehlina; Pa: Palmatolepis; PI: Polygnathelllls; Po: Polygnathus; Ps: Pselldopolygnathlls. B Percentage distribution
of conodont genera in the Sentiero Storico A (SSA) section. Genera abbreviations as in Figure lOA.
portion of the section (referred to the Lower expansa
Zone) to be regarded as pa-po biofacies. Also this
part of the section displays a local tectonicallydriven regression; this is in contrast with the global
transgression. The second half of the section,
referred to the Middle expansa-Lower
has been
to the pa-bi biofacies; it is
consistent with the global
trend.
Section SCV ranges from the Upper expansa Zone
to the Upper praesulcata Zone (Figures 11 A-B). The
Middle praesulcata Zone has not been discriminated
by biostratigraphic analysis. It was not possible to
define the Middle praesulcata Zone using conodont
faunal associations from the Carnic Alps. In our
view recognition of this biozone, defined by
disappearance of taxa in a context of low faunal
frequency, is very difficult. Over (1992),
incidentally, disregards the Middle praesulcata Zone,
regarding it and its base as being unrecognizable.
We agree with Over's opinion. Sample SCV3, here
referred to the Lower praeslllcata Zone because of
the presence of Protognathodlls collinsoni Ziegler and
Protognathodlls meisclmeri Ziegler, could also have
been assigned to the Middle praesulcata Zone. Since
unequivocal biostratigraphic assignment of sample
SCV3 was not possible, the biofacies datum (po
biofacies) was not included in Figures 5-7. It is
stressed that the two uppermost samples, SCV4 and
314
M.C. Perri, C. Spalletta
A
B
Sentiero per Cresta Verde (SCV)
Sentlero per ('resta Verde
SCVI SCV2 SCV3 SCV4SCV5 Total
Samples
cm above base
8
Weight (g)
115
1075 2710
201
268
2700 2360
145
780
Species
H,
4,1U~
1.7
Br
2.3
22.3
S.U
Pa
27.9
43}~
S,n
1.0
Bi. aculeatus
Pa
5
5
Po
2.3
2.5
f15JJ
kJ.K
Bi. costatus M2
Pa
9
9
Pr
25.11
105
!:'Ul
2',l.X
Bi. ultimus M2
Pa
7
Br. suprema
Pa
I
24
25
7
Pa. grac. gracilis
Pa
12
23
37
Po. marginvolutus
Pa
I
Ps. brevipennatus
Pa
I
Ps. marb. trigonicus
Pa
7
Ps
1.0
SI
Scnlic(() per
I
Pa
I
I
Pa
I
2
Br. fissilis
Pa
3
3
Pa. grac. sigmoidalis Pa
30
30
Pa
Pa
3
Pr. collinsoni
Pr. meischneri
Pa
3
I
Pa
2
4
Po. purus purus
Pa
88
Pr. kockeli
Pa
6
Si. praesulcata
Pa
I
2
3
Ps. primus
Pa
4
4
8
2
2
105
39
328
13
25
20
38
4
6
6
94
6
Pa
121
HI)'!;:
3
Po. inomatus
Po. corn. communis
43
Ver<..!c (SCV)
43
36
Bi. sp.
Total
Cr~~s!<.l
I
Bi. ultimus Ml
Po. corn. carina
Figure 11
(S('V)
I u. expansa IL. prae.1 u. praesul.l
Zones
SCV I SCV2 SCV) SCV4 SCV5
Numerical values, biozonal and biofacies assignments and computer generated diagram. A: Numerical
distribution of conodont taxa in the Sentiero per Cresta Verde (SCV) section. Bi: Bispathodus; Br: Branmehla;
Pa: Palmatolepis; Po: Polygnathus; Pr: Prothognathodus; Ps: Pseudopolygnathus; Si: Siphonodella. B: Percentage
distribution of conodont genera in the Sentiero per Cresta Verde (SCV) section. Genera abbreviations as in
Figure llA.
SCV5, referred to the Upper praesulcata Zone by the
presence of Protognathodus kockeli Bischoff, have
been assigned to the po biofacies; they represent the
praesulcata global regression Zone.
Biostratigraphic analysis indicates a gap in section
PZc. This is due to a fault eliminating part of the
sequence corresponding to the Lower-Upper
duplicata Zone; it divides the section into a lower
portion (PZC1-PZC4) referred to the sukata Zone,
and an upper one (PZC5-PZC12) assigned to the
sandbergi Zone (Figure 12 A-B).
The samples referred to the sulcata Zone were
assigned to the po biofacies because of the
extremely high percentage of Polygnathus. This
biofacies, characteristic of outer shelf environments,
is indicative of the sulcata Zone regression in the
Carnic Alps. The sulcata Zone regression is
expressed in other European areas (Bless 1993; Bless
et al. 1993); this contrasts with the global
transgression at the base of the Carboniferous (Ross
and Ross 1988).
The siphonodellid biofacies prevails in the portion
of the section referred to the sandbergi Zone.
Increase in the percentage of Siphonodella during the
sandbergi Zone transgression is reported from other
European areas (Bless 1993; Bless et al. 1993) and
from northeastern Australia (Talent 1989: Mawson
and Talent 1997).
CARNIC ALPS SEA-LEVEL CURVE
Analysis of the data from the Famennian-middle
Tournaisian sections of the Carnic Alps allows
inference of a qualitative regional sea-level curve
(Figure 13). This can be compared with the
Euramerica Devonian sea-level curve proposed by
Johnson et al. (1985) and later modified by Johnson
and Sandberg (1989). The early Tournaisian portion
of the local sea-level curve has been compared with
the coastal onlap curve - reflecting eustatic sea-level
changes - proposed by Ross and Ross (1988) for the
Carboniferous and Permian. Our data have also
been compared with data for the same time interval
from northeastern Australia (Talent 1989; Mawson
and Talent 1997) and from northwest Africa (Wendt
and Belka 1991).
Devonian-Carboniferous T-R pattern in the Carnic Alps
A
315
Plan di Zermula (PZC)
I
Zone!>
Samples
cm above base
I
sulcala
I
sandbcrgi
PlCI PZC2 PlC) PlC4 JYZC5 PlC6 PZ(7 PZC8 PZC9 PlCIO PlCl1 JYZCI2 Total
4
18
48
61
71
78
28
35
81
113
125
134
Welghl (g)
4750
5410
2325
)075
4980
2100
3180
13
72
6725
1825
2120
4675
)()()()
Species
Po. corn. communis
Pa
2
Po. purus purus
Pa
2)0
44)
440
388
125
3
1935
10
20
22
4
2
6
18
Pr. kockell
Pa
30
5
16
51
Pr. meischncn
Pa
20
10
4
)4
Ps. primus
Pa
2
8
6
24
Si. praesulcata
Pa
10
12
Si. sulcata
Pa
2
5
Vo. sp.
Pa
11
Bi. aculeatus
Pa
I
Po. longiposticus
Pa
Bi. sp
Pa
Po. sp
Pa
Pi. valdecavalus
Pa
Po. n. sp. B Gedik
Po. inornatus
Po. sp. P.
70
22
23
12
16
58
34
I
4
15
24
65
11
13
2
2
15
32
176
I
4
2
I
10
I
18
Pa
7
2
21
11
54
Pa
10
2
16
2
Pa
14
Po. radinus
Pa
35
28
14
32
Ps. sp. M
Pa
2
4
I
I
Ps. friangulus
Pa
70
8
30
94
30
36
51
319
37
46
22
109
8
Pa
1108
160
680
115
54D
569
51
3225
Pa
566
73
350
31
272
373
7
1672
Si lohata
Pa
6
3
8
59
7
13
18
119
Si.obsoleta
Pa
10
6
27
19
10
80
Si. quadruplicata
Pa
243
56
112
16
76
63
7
573
Si. sp.
Pa
152
36
100
18
125
132
8
572
Ps. fusiformis
Pa
2
Ps. marginalus
Pa
I
BI. stabilis
Pa
I
I
Po. sp. A
Pa
6
9
Po.sp.B
Pa
2
I
3
Po. perplanus
Pa
2
2
4
Has~
1,1
I
9
320
511
485
1.7
0,1
11,2
n,R
n,t}
1.7
6.3
0,1
0.4
20,2
21.9
7,1
13.0
22.7
2,7
2,'
19,9
H.5
89.4
xLi
44,5
0.6
0,1
\)5,3
I}O.7
8.3
17,5
0.6
3.7
0.4
5,7
I.'
1,0
IJ
31
2,2
2.7
IIl.O
',8
3.3
1.5
91.2
87.9
50,7
0,9
2.2
81.8
0,1
453
2376
364
1433
588
Figure 12
7.7
0.7
8\),0
0,3
5,2
2
Pa
77,2
:'.1
65
15
6
PlCI fYLC2 PZC.1 PZC4 PZCS Pz'Ch PZC7 PZeB PZC!) ?Zelo PZCII PZCl2
Ps
2.3
15
Plan di Zermula C (JYZC)
S,
Vo
LU
Pa
Total
0,2
56
Pa
Si. sp. juv.
PI
Po
P,
2
17
Po. purus subplanus
Si. cooperi M2
B,
J)
Pr. collinsoni
Si. duplicata sensu.
B
)
34.4
0.2
12,5
1
32
1148
1404
I
11
256
9370
Numerical values, biozonal and biofacies
assignments and computer generated
diagram, A: Numerical distribution of
conodont taxa in the Plan di Zermula C
(PZC) section, Bi: Bispathodus; Pi:
Pinacognathus; Po: Polygnathus; Pr:
Prothognathodus; Ps: Pseudopolygnathus; Si:
Siphonodel/a; Vo: Vogelgnathus, B: Percentage
distribution of conodont genera in the Plan
di Zermula C (PZC) section, Genera
abbreviations as in Figure 12A.
Plan di Zermula C \PlO
lOO";;
Oq
~
~
~
~
~
~
~
"u
t:
@
~ '"~ ~ 8
'"
It is worth recalling that the Carnic basin
underwent deepening from the upper Frasnian to
the Bashkirian. Geological data - slumping, thin
turbiditic layers and breccias - indicate that the
basin was affected by intense tectonic activity from
the upper Frasnian to the middle Famennian
(Uppermost marginifera Zone). Lack of geological
data bearing on tectonic activity leads us to
presume that the Camic basin was characterized by
stable depth during the second half of the
Famennian and lower Toumaisian. This is despite
persistence of a pronounced trend towards
transgression regionally.
The local sea-level curve can be subdivided into
three intervals: 1) Upper rhenana-Iinguifomlis Zone
interval, 2) Middle triangularis to Uppermost
316
M.C. Perri, C. Spalletta
SYST. STAGE
T.
S.
CONOOONT
ZONE
C.
Z.
Lower crenulata
i
0
I:Q
~
<C
U
Cl)
.....
~
sandbergi
~
Upper duplicata
0
Lower duplicata
Z
;:J
Eo--
-~
Z
0
expansa
--
marginifera
U+f
~
rhomboidea
--
>
~
crepida
triangularis
Q
Cl)
Z
tinKul!Ormis
rhenana
;amleae
hassi
~
punctata
lJ..
transitans
Z
~
.....
~
falsiovalis
Figure 13
-
trachytera
:;
\
(Johnson et al. 1985. modified
by Johnson and Sandberg 1989)
UJ
Z
Z
I--
\
-
~
::5
-
-- --
~
"--
-
""
T
)
-
~
I--
L
,
-
I--
\
T-R Curve for Euramerica
-
postera
I--
\
sulcata
~
.....
J
\
\
praesulcata
Z
Carnic Alps sea -level curve
)
<
S
~
\
"
--RISE
FALL_
I-III-III-II--
~
II-
~
,....
,....
!--
-
,..-
lI-!-I!-!--
--
I-'--
c--
Carnic Alps sea-level curve inferred by conodont biofacies analysis. For comparison the Euramerica
Devonian sea-level curve proposed by Johnson et al. (1985 and modified in Johnson and Sandberg 1989) is
presented. Conodont zonation by Ziegler and Sandberg (1990) modified.
marginifera Zone interval, and 3) Lower trachytera to
sandbergi Zone interval. Biofacies analysis of spot
transgression-regression cycles of the trachyterapostera zones and the expansa-praesulcata zones. The
data for the first interval seems to indicate a
regressive event in the upper part of the Upper
rhenana Zone to the lower part of the linguiformis
Zone. The second interval of the Carnic Alps sealevel curve is consistent with a persistent
transgressive trend
except for the Upper
rhomboidea Zone where a regressive trend seems
more or less recorded. The regressive events of the
Lower rhomboidea-Lower marginifera Zone and of the
Upper marginifera-Uppermost marginifera Zone of
Euramerica are not apparent, doubtless due to the
drowning of the Carnic Basin. The only exception,
as noted above, is the Upper rhomboidea Zone when
it seems that the effects of the Euramerica regressive
event offset those of the local transgressive trend.
The third interval displays two significant
transgression-regression couples followed by a
transgressive event at the end of the interval. The
local sea-level curve is in accord with the
Euramerica sea-level curve for the Devonian, and
for the Early Carboniferous; it shows the same
regression-transgression trend reported from other
areas for the same interval. Thus, in the Carnic Alps
the carbonate sequence for this time interval
corresponds closely with the Euramerica
only exception, as regards the Carnic Alps, is
during the Lower expansa Zone when a tectonicallydriven local regression occurred, contrasting with
the global transgression at this time. The local
Lower expansa Zone regression also contrasts with
the major basinal transgressive trend at that time.
The Middle and Upper praesulcata Zone regression
continued into the sulcata Zone, as reported for
other European areas; it contrasts with the global
sulcata Zone transgression.
The transgressive event in the sandbergi Zone
coincides with those of other European areas and of
northeastern Australia.
CONCLUSIONS
Application of biofacies analysis has enabled
recognition of changes in associations of conodont
genera, even in the monotonous micritic sequence
of the clymenid and goniatitid limestones of the
Carnic Alps during the late Frasnian-middle
Tournaisian time interval.
In the micritic facies, biofacies changes from deep
to less deep reflect regressive events. By means of
conodont biofacies analysis four regressive events
Devonian-Carboniferous T-R pattern in the Carnic Alps
317
are reported, clearly reflected in the sea-level curve
inferred from data from the Carnic Alps.
Comparison of the local sea-level curve with those
proposed for the Devonian and for the
Carboniferous, together with data from North
Africa and Australia reveals the following results:
1) In the Carnic Alps the Euramerica regressive
trend from Upper rhenana to linglliformis Zone
seems to be represented.
2) The local sea-level curve from Middle
triangularis to Uppermost marginifera Zone indicates
a transgressive trend due to drowning of the Carnic
Basin. This appears to have masked the
Euramerican regressive events during the
rhomboidea-marginifera zones. Only in the Upper
rhomboidea Zone does the Euramerican regression
seem to be recorded in part.
3) The Carnic Alps sea-level curve during the
Lower trachytera-sandbergi zones time-interval is
completely comparable with the Euramerica
Devonian sea-level curve, with data for the
Carboniferous from other European areas,
northwest Africa and northeastern Australia. That
the global T-R events are reflected in the Carnic
Alps calcareous sequence is due to tectonic stability
of the basin. The global regressions of the postera
and praesulcata zones can be discriminated. It is
worth noting that in the Carnic Alps the postera
Zone regression continues into the Lower expansa
Zone. This local regression in the Lower expansa
Zone is tectonically-driven.
The praesulcata Zone regression in Euramerica and
northwest Africa extends into the sulcata Zone, as it
does in other European areas; it contrasts with the
global transgression of the base of the
Carboniferous.
The sandbergi Zone transgression reported in other
European areas and in northeastern Australia is
reflected in the clymenid and goniatitid limestones
of the Carnic Alps.
and the distribution of the ostracode taxon
PsclIdoleperditia gr. venlllosa. Annales dc la Socit'te
geologiqllc de Belgique 115(2): 475-481 [imprint 1992].
ACKNOWLEDGEMENTS
Much of the research was funded by MURST and
CNR grants to M.C. Perri. The manuscript has
benefited from precious advice, reviews and editing
skills of Professor John Talent, A/Professor Ruth
Mawson and an U1mamed assessor; we heartily
thank them for their time and interest. We thank
Dr. Beniamino Costantini who made or improved
most of the computer-generated figures. This is a
contribution to IeCp Project 421 North Gondwana
rnid-Palaeo2oic bioevent/biogeography patterns in
relation to crustal dynamics.
REFERENCES
Bless, M.].M. (1993). Comparison between eustatic T-R
cycles around the Devonian-Carboniferous boundary
Bless, M.].M., Becker, R. T., Higgs, K., Paproth, E. and
Streel, M. (1993). Eustatic cycles around the
Devonian-Carboniferous boundary and the
sedimentary and fossil record in Sauerland (Federal
Republic of Germany). Annales de la Societe geologique
de Belgiqlle 115(2): 689-702 [imprint 1992].
Dreesen, R.]. (1992). Conodont biofacies analysis of the
Devonian/Carboniferous boundary beds in the
Carnic Alps. Jahrbuch dcr Gcologisclze BlIndesanstalt,
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