Geological Quarterly, 2004, 48 (1): 83–88
Very large stromatoporoid indicating Early Frasnian reef core
(Holy Cross Mts., Poland)
Grzegorz RACKI and Ma³gorzata SOBSTEL
Racki G. and Sobstel M. (2004) — Very large stromatoporoid indicating Early Frasnian reef core (Holy Cross Mts., Poland). Geol.
Quart., 48 (1): 83–88. Warszawa.
A large stromatoporoid Actinostroma cf. crassepilatum Lecompte, 1951, at least 8.5 m in diameter and 0.85 m in height, occurs in the
Œluchowice quarry in Kielce, Holy Cross Mountains. This sponge occurs in growth position within Early Frasnian (transitans Zone)
intraclast-rich reef-rubble deposits. A unique preservation of the reef-builder close to a reef core is implied for the northern flank of the
developing Dyminy Reef during its maximum expansion northward into the Kostom³oty intrashelf basin.
Grzegorz Racki, Ma³gorzata Sobstel, Faculty of Earth Sciences, University of Silesia, Bêdziñska 60, PL-41-200 Sosnowiec, Poland;
e-mail: racki@us.edu.pl, sobstel@wnoz.us.edu.pl. (received: October 15, 2003; accepted: January 5, 2004).
Key words: Stromatoporoidea, Dyminy Reef, Frasnian, Holy Cross Mountains, Poland.
INTRODUCTION
Devonian exposures in the Holy Cross Mountains, Central
Poland (Fig. 1A and B) have provided important data on
stromatoporoid-coral facies of the globally occurring Frasnian
reef complexes; see for example KaŸmierczak (1971),
Szulczewski (1971), Narkiewicz (1988), Wrzo³ek (1988),
Nowiñski (1992) and Racki (1992). Stromatoporoids were
among the dominant reef builders on extensive Middle
Palaeozoic carbonate shelves (Wood, 1999). This extinct group
have been interpreted recently as a class of non-spiculate
sponges (Stearn et al., 1999), represented as fossils by their
basal carbonate skeleton (but see stromatoporid stromatolites
of KaŸmierczak, 2003). Stromatoporoids from the Holy Cross
Mountains Devonian succession have been comprehensively
described by KaŸmierczak (1971, 2003), while some palaeoecological aspects are discussed by £uczyñski (1998, 2003).
An exceptionally large stromatoporoid specimen in growth
position is described here as a record of a stromatoporoid-coral
reef-core. This unique occurrence, first noted in Racki (1992, p.
128), is considered in the context of facies pattern within the
Frasnian Dyminy Reef complex (Narkiewicz, 1988;
Narkiewicz et al., 1990; Racki, 1992).
PALAEOGEOGRAPHIC AND STRATIGRAPHIC
SETTING
Two distinct palaeogeographic-tectonic Devonian domains, the Kielce palaeohigh region and £ysogóry palaeolow
region, coupled with the transitional Kostom³oty area, characterise the Holy Cross Mountains part of Laurussian shelf
(Racki, 1992). The subsymmetrical facies plan is emphasised
by the central location of the Frasnian Dyminy Reef (Fig. 1B),
surrounded by deeper intrashelf basins: Chêciny–Zbrza (southern) and £ysogóry–Kostom³oty (northern), as summarised in
Narkiewicz (1988), Racki (1992) and Szulczewski (1995). Developmental stages of the stromatoporoid-coral reef ecosystem,
which collapsed near the Frasnian–Famennian boundary (see
summary in Copper, 2002), are in an overall accordance with
the Euramerican sea-level curve of Johnson et al. (1985).
A succession of varied Frasnian limestones (Kostom³oty
Beds in Szulczewski, 1971), developed close to the northern
periphery of the Dyminy Reef, is perfectly exposed in the abandoned Œluchowice quarry, located in the NW part of Kielce
(Fig. 1B and C). The locality is well-known due to well exposed folding and other tectonic phenomena seen there
(Lamarche et al., 1999), but not very attractive in
palaeontological terms because fossils only occur commonly in
84
Grzegorz Racki and Ma³gorzata Sobstel
Fig. 1. A — location of Œluchowice quarry in Poland, B — the Holy Cross Mountains (based on Racki, 1992, fig. 2), C — general lithological column
of the lower part of Œluchowice section (Szulczewski, 1971, fig. 7, modified), D — detailed succession of the Wietrznia Beds with the marked
stromatoporoid reef at western end of the Œluchowice quarry (Racki and Bultynck, 1993, fig. 4, modified)
The £ysogóry Region is shown to be limited to the £ysogóry basin sensu Racki (1993), i.e. bordered by the Holy Cross Fault, but a basin facies was
also partly developed in the Frasnian intrashelf basins surrounding the Dyminy Reef
B
Fig. 2. A — northern part of the eastern wall, western Œluchowice quarry at Kielce; studied part of the exposure arrowed (see
Fig. 2B); B — northeastern wall, with arrowed stromatoporoid (Actinostroma) reef (Ac) in the basal interval B of the
Wietrzna Beds, 0.8 m thick (see Fig. 1D)
Very large stromatoporoid indicating Early Frasnian reef core (Holy Cross Mts., Poland)
85
Bthe lowermost (described below) and uppermost parts, in the
Frasnian–Famennian interval where corals, brachiopods, crinoid debris are found (Szulczewski, 1971; Nowiñski, 1992;
Racki and Baliñski, 1998). Therefore, the coarse-grained,
fossiliferous and intraclast-rich limestones under study are a
distinctive variety of the generally fossil-impoverished
deep-slope facies, and re-assigned therefore to the Wietrznia
Beds by Racki and Bultynck (1993), characterised by intermediate facies position between fore-reef and basin settings (see
also Racki, 1992). This interval, ca. 4 m thick, occurs in the
northern part of the quarry (Fig. 2) and on the nearby Czarnów
Hill to the west (Szulczewski, 1971), and is precisely dated by
conodonts to the Early Frasnian Palmatolepis transitans Zone
(Racki and Bultynck, 1993).
IN-PLACE OCCURRENCE OF THE LARGE
STROMATOPOROID
In the western Œluchowice quarry, protected as a geological
reserve, the Wietrznia Beds crop out in subordinate northeastern wall, close to the quarry floor (Fig. 2A). The horizontally
arranged thick limestone layers form the lower limb of the
overturned Œluchowice fold (see Lamarche et al., 1999). The
oldest set A sensu Racki and Bultynck (1993), over 4 m thick,
contains several fossil-poor calcarenites in a marly-shale succession with abundant rhynchonellid brachiopods assigned to
Phlogoiderhynchus polonicus (Roemer) and Styliolina
domanicense Lyashenko and S. ex gr. nucleata Karpinsky (see
Biernat and Szulczewski, 1975; Haj³asz, 1992), as well as
branched corals in some layers (Fig. 1D). This interval is questionably placed in the lower Wietrznia Beds in the
Œluchowice-Czarnów succession due to its transitional nature
to the underlying Szyd³ówek Beds (Racki and Bultynck, 1993),
and this Givetian to Frasnian rhythmic marly unit is poorly exposed in the railway cuting to the north. The succeeding light
gray biointrarudites, with dark calcarenite, 0.3 m thick, at the
bottom (interval B), are marked by abundant reef-builder debris, mostly diverse dendroid and massive stromatoporoids and
corals, especially alveolitid tabulates (see list of taxa in
Nowiñski, 1992). The reef breccia is associated predominantly
with brachiopod and echinoderm (chiefly crinoid) bioclasts,
calcispheroids and other microproblematica, as well as with
unsorted micritic intraclasts (with peloidal-lumpy to spongy,
Fig. 3. A — close-up of the reef layer (northern part) built of in situ
Actinostroma (Ac, see Fig. 2B) and reef rubble (rr), note the indistinct
hemisphaerical-coalesced appearance of the stromatoporoid sheet; B —
photomicrograph of the peripheral part of the Actinostroma skeleton, with
visible poorly sorted intrabiosparenite enclosing sediment (see also
biointrasparudite microfacies in Szulczewski, 1971, pl. 26: 1), and
non-enveloping growth pattern
renalcid-like fabrics in places), including large flat pebbles in
conglomeratic beds (see Szulczewski, 1971, p. 60–61, pl. 24: 2,
pl. 26: 1 therein; Fig. 3B).
The second bed of interval B, 0.7–0.9 m in thickness, shows
a stromatoporoid skeleton in growth position along most of the
exposure, i.e., over a distance of ca. 12 m (Fig. 2B). The almost non-weathered rock surface, partly covered with ferric
oxide and an organic coating, is inconvenient for detailed observations, but the stromatoporoid apparently continued laterally over at least 8.5 m. Sorted fine-grained, as well as unsorted
talus-like deposits are found as the enclosing lithology, and the
Fig. 4. Actinostroma cf. crassepilatum Lecompte, 1951 from the Early Frasnian Wietrznia Beds at Œluchowice quarry
(see Fig. 1D); A — longitudinal section, B — obliquely-tangential section
86
Grzegorz Racki and Ma³gorzata Sobstel
Table 1
Dimensions of reticular tissue elements for Actinostroma cf.
crassepilatum Lecompte, 1951 from Œluchowice (Fig. 4)
Laminae
Pillars
max/2 mm min/2 mm thickness max/2 mm min/2 mm
10
7
0.06–0.14
7
5
thickness
0.18–0.29
moderately irregularly undulose upper contact between the
pale stromatoporoid skeleton and the coral-rich biosparudite is
clearly visible in the higher portion of the bed in some places
(see Figs. 2B and 3). The largest stromatoporoid thickness
(0.85 m) is noted in the middle part of the wall, but the partly
erosional vs. burial nature of its top is unrecognised due to its
poorly visible, probably non-enveloping growth pattern (sensu
Kershaw, 1998). The low-relief profile and non-enveloping
growth are typical of large examples of “massive”
stromatoporoids (£uczyñski, 2003).
Thin sections from two outer parts of the stromatoporoid
indicate assignment to the genus Actinostroma (Fig. 4). Despite differential recrystallization in both skeletal fragments,
highly thickened pillars (up to 0.3 mm; Table 1) are seen in the
reticular tissue. Therefore, a large tabular actinostromatid
specimen is implied to be the rock-former of the layer under
study, even if coalescence of several laminar individuals into
one large mass is likely (cf. Kershaw 1998, p. 523). When
compared with species described by KaŸmierczak (1971,
2003) from coeval strata of the Holy Cross Mts., this specimen is assignable only to A. crassepilatum Lecompte, 1951
(see KaŸmierczak, 1971, p. 137, pl. 40: 3, pl. 41: 6; 2003, p.
696, pl. 393: 3), widely distributed in European
Givetian–Frasnian carbonate complexes. Notably, this single
Actinostroma species has been determined by KaŸmierczak
(1971, 2003) in the Wietrznia Beds (at the type locality), as
the largest of the stromatoporoids there (up to 1.3 m in diameter and 0.75 cm high).
FINAL REMARKS AND IMPLICATIONS
FOR THE DYMINY REEF
Meter-sized autochthonous Actinostroma sponge skeletons
are not rare, because this genus is the commonest frame builder
of the Givetian to Frasnian stromatoporoid-coral reefs worldwide (Stearn et al., 1999, p. 33). However, its dimension is
noteworthy: the speciemen described here is the largest
stromatoporid reported so far from the Upper Devonian deposits from Poland. However, a giant tabular example of
Actinostroma expansum (Hall and Whitfield, 1873), ca. 1.5 m
high and 30 m wide, has been reported from the middle
Frasnian Shell Rock Formation (Nora Member) of Iowa
(Stock, pers. comm., 2003). Wood (2000) also described remarkably large actinostromatids from the Western Australian
Frasnian reef that can reach sizes of up to 5 m in diameter and
1.5 m in height. The Australian species A. windjanicum
Cockbain, 1984 is marked by highly complex
platy-multicolumnar growth, which may be presumed also for
the incompletely exposed specimen from Œluchowice (see Fig.
3A) that stabilised skeletal debris and fine-grained substrate.
A widespread Actinostroma assemblage was discerned by
Racki (1992, p, 128) as a principal ecological component of the
wave-resistant accretion rim of the Dyminy Reef in fairly agitated waters at most 10 m below sea level, but most “massive”
stromatoporoid occurrences are post-mortem hydrodynamically reworked (KaŸmierczak, 1971; Narkiewicz et al., 1990;
£uczyñski, 1998, 2003). Findings of large in situ
stromatoporoid skeletons are quoted by Szulczewski (1971, p.
86) and Racki (1992, p. 128), also from talus-like
Stromatoporoid-Detrital Beds. Szulczewski (1971, p.
107–112) broadly discussed some basic limitations of reef recognition in this region, and he concluded that “part of detrital
limestones with large-sized stromatoporoids make up an actual
reef core” (Szulczewski, 1971, p. 112). In fact, a common feature of fossil reefs which represent diverse and complex
biogenic structures, is a low preservation probability of the
wave- and storm-agitated accreted rim formed by essentially in
situ skeletons (e.g. Hoffman and Narkiewicz, 1977; Longman,
1981; Wood, 1999; Riding, 2002), even if an alternative (ramp
model) explanation was highlighted by Stanton and Flügel
(1995; see also Machel and Hunter, 1994).
In the case of the Wietrznia Beds under study, reef-rubble
intraclastic deposits have continued both to the east (eastern
Œluchowice quarry) and west (Czarnów Hill; Szulczewski,
1971; Racki and Bultynck, 1993), but the autochthonous
frame-builders are limited to the western Œluchowice locality
only. The spectacular in situ growth of Actinostroma cf.
crassepilatum indicates that this species seems to live preferably in turbulent habitats that appeared to be optimal to support
huge reef-building organisms. This unique framestone layer
determines a portion of the Early Frasnian Dyminy Reef, representing a true reef-core (cf. Szulczewski, 1971) or at least very
proximal fore-reef facies, during its extreme progradation
northward into the £ysogóry–Kostom³oty basin. Notably, this
initial developmental phase of the reef-complex (= foundation
stage of Racki, 1992) was associated also with the ephemeral
appearance of the distinctive Kadzielnia-type mud mounds on
gentle irregular reef flanks, marked by sheet-like stromatoporoid mud binders (KaŸmierczak, 1971; Szulczewski, 1971;
Racki, 1992; £uczyñski, 1998). This suggests strongly hydrodynamically changing conditions over the differentiated
bioherm-fringed margin of the early “table”-type Dyminy Reef
(Szulczewski, 1971; Racki, 1992). Northward progradation on
a similar scale has been recorded only for the final reef-cap developmental stage of the latest Frasnian (see Narkiewicz, 1988;
Racki, 1992; Racki and Baliñski, 1998).
Acknowledgements. Carl W. Stock is kindly acknowledged for constructive comments on the manuscript, and Jan
Malec for useful editorial remarks. M. Racka provided the
photo for Figure 2A. We thank M. Lewandowski for digital
preparation of figures. This work has been partly supported by
the State Committee for Scientific Research (KBN grant 3
P04D 040 22 for G. Racki) and the Silesian University.
Very large stromatoporoid indicating Early Frasnian reef core (Holy Cross Mts., Poland)
87
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