Geological Quarterly. Vol. 39. No.4. 1995, p. 471-488
Michal SZULCZEWSKI
Mts.
The Devonian and Early Carboniferous succession in the Holy Mts. records a steady sea level and bounded by major angular unconformities. The Lower Devonian is a terri genic sequence of complex.
continental and shallow-marine facies. Growth of a shallow-marine platform in the Middle to sep.araljon of two adjacent intrashelf basins. This central swell was stepwise traristorrn<~d
and influenced a pattern of facies and thickness after its completed in the imn,re.<;!;ive progress is noticed in of sedimentation and stmtigmphy of the carl[)On,ate
INTRODUCTION Cross Mountains
IJa.LU .... '.JlUl po:Sltlon makes
palae()te(~tolmcal re:COlllstIllCI:rorIS, which extend far from this The aim of this article is to offer an outline of d.elpmHtlOn,al
of the HCM in the Devonian and Carboniferous and to review the eXlstll1lg literatulre, in order to facilitate geology of this selected pm)1W)ns could be included in since the literature I'n,,,,.,.,,..-.... , ....
modified and Up'-."L'-,""
ranls-t::;urop(~an Suture Zone
w
()rJcimOiDThe Devonian and the Carboniferous make a coherent of a aelpm,lnOnial history in the HCM area, since this stratigraphic succession is bounded by the major angular unconformities. They correlate with the late Caledonian and the Variscan orogenies, but effects of the two tectonic events are much more mild than in regions of their typical development. The stratigraphic succession records a steady sea-level rise since the Devonian till the Early Carboniferous. Particularly, no remarkable regression is noticeable in the Famennian, in contrast to the Rheinisches Schiefergebirge and the Ardennes, and even to the of the eustatic sea-level curve proposed by J. G. Johnson et al. (1985).
A feature of the pattern in the Palaeozoic of the HCM is its twofold
U..-":H./j""" diversification (Fig. It resulted from a different palaeotectonical behaviour of
The northern of them is caned and the southern one - reQ:arClea in the two ways: (1) as recent regional tectonic entities and (2) as to their first "",""'r·"t~nrtln ....
their boundary is positioned Cross Fault (HeF). This definition is aC1(lpte:d in this paper because of its defined in the second way shifted in time and the Devonian was situated more or less south of the HCF.
THE LO'NER DEVONIAN CLASTIC DEPOSITION
The Lower Devonian in the area of the HCM is developed mainly as a distinct terrigenous sequence, composed of fine clastics. It reveals significant differences in its thickness, record and vertical facies succes-
sion when In it follows
the marine Silurian and a sequence of stratigraphic stages.
Its thickness is there and a record of marine facies at least better readable than in the Kielce where it is two times or more conspicuously mCOITlpllere at its base and unconformable to the folded Lower Palaeozoic. The Lower Devonian
re}~arljed as the most illustrative feature of the twofold Cross area in the Palaeozoic.
LOWER DEVON rAN IN THEt,YSOG6RY REGION
In the marine facies continues from the Silurian up to the lowermost pronouncely with the base of the terrigenous dls:appeli( westward. the lower of the renng1enc)Us
("I"II-nnl.o'l<' is diachronous within the Gedinnian .
• ' .... ".5' ... ".'''''-' complex (G6zd in the Lysog6ry region) is up to about 550 min
Lobanowski, 1981). It displays a vertical facies evolution in a generally upward increasing participation and thickness of an increasing maturity of their mineral composition and a change of colouring from usually brown and cherry to more light. It is associated with an evolution of a fossils content, vertically increasing in amount, diversity and participation of marine components. The commonly
Depositional evolution of the Holy Cross Mts .. _ 473
... Y'."''' .... ,.,I subdivision of the cornplex, Barcza and
1-<r\'rYn,,,h/u,,,, reflects the main of its facies de'JeL()prnerlt.
The lack of sufficient OlOlsrraUJgrapnllC Lower Devonian
sequence an accurate chlronOSltra1~1,gI~apnlC subdivision of the Lower Devonian succession even at the level. The best dated
which were de()OSllted in marine environments.
tionoftheBostowBeds benthic trilobites
The age of the Klon6w and Barcza Formations determined. A difference of at least a half of a is by various pos:mcm of these units. The Klonow Formation is
the Gedinnian (J. the
or to both Gedinnian and Lower :)le:gemaln ass,lgrled to the
or to the Lower Emsian Formation is attributed to the pallae'On1[Ol()glcal evidences (H. Lobanow*
ae[)oSmOlnal environments of the Klon6w and Barcza Formations are not sufficient- ly understood. In their characteristic the two
~rH~r.;:."'I\I fossiliferous. contain only scarce plaCOClenn sp()ramc bivalves or remains.
The Klon6w Formation is orOlWfl-re;OOlsn. thin-bedded and contain
wackes, ascribed to the continental Old Red Sandstone
rt:>f't:>nth. H. Lobanowski them as fluvial overbank
and contains well individualised sandstone sets
evidenced the three marine intercalations ,.."" .. v"rt""rI
Czarnocki (1 stenohaline marine taxa from the Barcza Formation.
These that bivalves are scattered the
delPo~;rte;d in the marine but also open marine.
tralnSJ2:reS:SlCiTI ol:::nrlHe,ly overflooded the :LV~i02orV
£.oJ .... ;;.. .... ,,""'..., Formation H. LOOar10\VS.I\:L
This formation is sandstone with its overall ratio to the other tenngl~nc)us
.... vlfJ'-""c..:> of about 4.5: 1. The vertical sequence reveals of several lithofacjes
aSS:OClatlons, re:prt~SeI1tlnlg the storm-dominated de~)OSltIOinal
are distinctive of
~
a
C/,DDO.O CJ a 4' Pi~
NORTHERN
KIELCE
CENTRAL
b ~ 77
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-
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....- - . c -
1- 1 ... ' -
ll. .', ., , ' .
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,'. . ' 4 , , , , .,., ... "
... .
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~$$~$~~~~~'~'~':5:' F :' '~'::::." : ; ::: :: : : :', ':::,:~;' ,. , .•••• ~. 1>:'; ""
bU
.....C~ d~
--~.' .-elll fm
j[2J k§±ftH
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, I [+::;:.,:,,'(,,:1mCJ ngg
SOUTHERN
"LI~~
,- ...,
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- -.
...,
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- - . -
"',g~ h~
O~ p[]]]]
Depositional evolution of the Holy Cross Mts ... 475
LOWER DEVONIAN IN THE KIELCE REGION
The thickness of the Lower Devonian in the eastern part of the Kielce region attains 260 m, but commonly is about 130-150 m (M. Tarnowska, 1981). In the westem part of the region it is usually no more than 30 m thick. Locally it is even attenuated to 2-3 m (J. Glazek etal., 1981; Z. Kowalczewski, 1971; M. Tarnowska, 1987).
The base of the Lower Devonian truncates the Lower Palaeozoic succession down to the Lower Cambrian. It is, however, noteworthy that the gap associated with this unconfor- mity is a cummulative effect of the erosional episode following the post-Cambrian uplift as well as the post-Silurian one. A differentiation of the Lower Devonian facies, thickness and probably also completness of stratigraphic record reflects the morphology of the inundated land (cf. 1. Glazek et al., 1981).
Drill record reveals that, in its more expanded development the sequence consists of alternating complexes dominated by sandstones or by mudstones and clays (e.g. Z. Kowal- czewski, 1971; M. Tarnowska, 1981). Over the eastern part of the region, where its stratigraphy is better understood, it consists of two mudstone complexes sandwiched with two sandstone ones. Conglomerates are subordinate to finer clastics and almost confined to the western part of the Kielce region (J. Czarnocki, 1936; Z. Kowalczewski, 1971). They are mostly basal conglomerates, but another level is situated within the unit (Bieliny conglomerate ).
Fig. I. Simplified diagrammatic cross-section through the Holy Cross Mts. from the Lower Devonian to Lower Carboniferous times
1 - Bost6w Beds; 2 - Klon6w Formation; 3 - Miedziana G6ra Conglomerate; 4 - Barcza Formation; 5 - Zag6rze Formation; 6 - Bukowa G6('a Shale Formation; 7 - Kapkazy Formation; 8 -Grzegorzowice Formation;
9 - Wojciechowice Formation; 10 - Skaiy Formation; 11 - Swi~tomarz Formation.; 12 - Pokrzywianka Beds;
13 - Nieczulice Beds and Sniadka Formation; 14 - Szyd16wek Beds; 15 - Laskowa G6ra Beds; 16 - Kowala Formation; 17 - Kostomioty Beds; 18 - Manticoceras Limestone; 19 - Radlin Beds; 20 - Zar~by Formation;
21 - Gal~zice Debrite Member ofLech6wek Formation; 22- Garno Beds; 23 - Gulacz6w Member ofLech6wek Formation; 24 - remaining portion of Lech6wek Formation; a - conglomerates; b - dominating coarse-grained clastics; c - coarse- and ftne-grained clastics; d - dominating fine-grained clastics; e - clayey and marly shales;
f - siliceous shales; g - marly limestones and shales; h - limestones and shales; i-nodular limestones; j - cephalopod limestones; k - condensed cephalopod and crinoidal limestones; 1 - micrites. calcarenites and calcirudites; m - calcirudites; n - massive nnd bedded limestone; 0 - dolomites; p - stratigraphic gaps Uproszczony przekr6j przez Gory Swi~tokrzyskie od dolnego dewonu do dolnego karbonu
I - warstwy bostowskie; 2 - formacja klonowska; 3 - zlepieniec miedzianog6rski; 4 - formacja barczanska;
5 - formacja zag6rzartska; 6 - formacja lupk6w z Bukowej G6ry; 7 - fonnacja kapkazka; 8 - formacja grzegorzowicka; 9 - fonnacja wojciechowicka; 10 - formacja skalska; Jl - formacja swi~tomarska; 12- warstwy pokrzywiru'iskie; 13 - warstwy nieczulickie i formacja sniadkowska; 14 - warstwy szydt6weckie; 15 - warstwy Laskowej Gory; 16 - fonnacja z Kowali; 17 - warstwy kostomtockie; 18 - wapieri mantikocera- sowy; 19 - warstwy radliriskie; 20 - formacja zarebiariska; 21 - ogniwo debrytow gatezickich formacji z Lech6wka; 22 - warstwy z G6ma; 23 - ogniwo gutaczowskie formacji z Lech6wka; 24 - pozostaia cZeSc formacji z Lech6wka; a - zlepience; b - skaty klastyczne z przewagll gruboziamistych; c - grubo-i drobno- ziamiste sknly klastyczne; d -skaly klastyczne z przewagq drobnoziamistych; e - lupki ilaste i marg)iste; f - tupki krzemionkowe; g - wapienie marg\i~te i tupki; h - wapienie i tupki; i - wapienie gru:dowe; j - wapienie glowonogowe; k - skondensowane wapienie glowonogowe i krynoidowe; I - wapienie mikrytowe, kalkarenity i kalcyrudyty; m - kalcyrudyty; n - wapienie masywne i warstwowane; 0 - dolomity; p -Iuki stratygraficzne
the Lower Devonian sequence this was termed plaCOClen:n sandstone" and attributed to the Lower Emsian (J.
SUJ:lpo:sed to be and Clej:)OSl.teCl
ACCor01nlg to recent papers, those differences seem 1981) suggests that the Devonian deT)OSitlcm commenced in the southern earlier than it was in the (jle:geJman.
She relies on the ter:;lhn)COrrelatl.on and one of the several found horizons as
[QJ:)m~:JSI part of the Barcza Formation in
M. Tarnowska 19811 also claims that the sequence accumulated in recurrent alluvial and marine nearshore environments. The southern succession indeed
but almost
Formation in
Pl3CO(lenm fishes are indeed the most characteristic fossils.
and bivaI yes (1. M.
environment of this facies",
L.B.N. noty~ade~qu,a[eIY
trace fossils found
the Emit of known occurrence of marine of the HCM.
-:>rh'''''',::.nt to the deserves attention. its would contribute to the vital
qu<~tJlon of the territorial consolidation of the HCM area in the Devonian times The of the Lower Devonian in this belt has U .... ~UH ... I J
much more in common with the pattern characteristic of the than that of
the Kielce one. It overlies the Silurian (1. J.
akin its northern r'1"\.n"ltp.1"T',,,ri
The
units seem to extend to this
the
of this belt is the
with its is as a main stratiform
its maximum thickness in excess of 45 and as its sateHite lenses. It consists of
n.-"·rlnrYI1,,,<> ... tl,, rounded cobbles and boulders of the Cambrian identified
rare Ordovician g18.UC10nJtlc
it: submarine fan
which consists of residual
lJeJ)OSIUOr.lal evolution of the Holy Cross Mts ... 477
was based cOIOgl.oDlerate within
the Klon6w Formation of continental is too
cornpJlca.teo and to be accepted.
There is a that a source area of components of the Miedziana G6ra Conglonrlerate were the Cambrian rocks in the nl"'"ltrTn,"rn
1971; I.
contradicts another observation of 1. Cz,arnoc~a,
graphJlcaJlj C()mIDlelte succession of Palaeozoic systems. as far as we there is no that it was available for erosion in the Devonian. Far more
that the Miedziana Gara is of material from
the Kielce where the Middle Cambrian was at the surface and a land
rnl"'"l.,.nr'I"'"Ilt"'lCHt could be at the of Devonian
sU1;ge~ste~d truncation of veneer of another I"'r\,nnll"'"l ... 'Ar<:lIrill>
the Gruchawka seems to
the Miedziana G6ra
de~)OSll tea after a in southern
THE LOWERJMIDDLE DEVONIAN BOUNDARY:
CESSATION OF CLASTIC DEPOSITION
""'''Prl'uin,n the Lower Devonian clastic sequence exhibit
The differen-
attributed to the latest Emsian and the Early Eifehan. This turnover
.. H F - , U I L l \ ... U l L rise of the relative sea level. J. Malec cf. S.
SU}:IDo:sed that it reflects the eustatic sea leval rise of the The introduced a domination aermsltlcm instead of hitherto
in the confines of the LowerlMiddle Devonian in the The differentiation of the facies of
the de[)OSlUOnal palae()toIJO~~raT)hy
ously distributed
while the areas where clastics are elevations.
The and limestones of this tra,ns~;re~;sn/e
abundant fossils of open marine biota. The
is characteristic of the Lower Eifelian of both the Kielce and overlie the clastic succession J. 199
SUJggf~tlng an existence of sub-basins with restricted circulation. In such rio,..."' ... , ... the of the Kielce
that the of the ten"lge,nmJS
and even
her "tuff bed T4" as a rp.CYH'I'n'!ll
correlative horizon situated close to the LowerfMiddle Devonian hr." .... rl"' .... , in the Kielce and farther to the south.
THE GROWTH OF THE MIDDLE-UPPER DEVONIAN CARBONATE PLATFORM
A substantial advance sea in the
of the relative sea level late in the Bifehan. The facies became SmlplltIe:a
UV~/V""HHJ'H was established over the vast Fennosarmatian
or::;IUnl!r::;I:.l. The "carbonate commenced its
of the shallow-marine carbonate The carbo- ae'vellOOlng until the Frasnian and attained a thickness of about 1400
were
dIagel1etJlc dolomites are common features 1991, S. M. Szul-
IJ~"LLVAJL< when it was also extended over the intra-shelf basinal facies.
The second and the third of ae'/eUJPrnerlt to the bank and reef
pli3tUOirm are similar
in the Devonian carbonate attributed the Frasnian. Both are repre-
make up a bulk of the carbonate
... U",UU,/',UIC>U\.A. as the Kowala Formation M. Narkiewicz et aL
Its thickness ranges from 330 to above 800 m and it {'rUTIn'nc~><I.
lations in situ. At least four del~pe,nlIllg were re(:o,Q:m~;ea
__ ~ .. I".,_~ in intennittent nT',. ... '''' ... , ... ,....
SYllCl'1trOllOliS correlation of the relati ve sea level ~"U'"f->'J'''
UeJ:loslltlOnal evolution of the Cross Mts ... 479
I-"<.I.~AVHU and the sea level '-'''',",H};;''"''''
1. O. Johnson et ai.
The bank commenced with accumulation of undifferentiated ::J·tllnJw(~eDnalus
biostromal bank which was the Sitk6wka bank cOlmplex
K.a~~mllerC~~aK, 1971; A.
two intra-shelf basins.
the most
In the Middle Frasnian the external parts of the carbonate were covered with detrital carbonate skeletal ooids and sediment binding Renalcis
eM.
M. This facies isstn)m,atopor'oicl-c()ral cornmunitv was serlOuSIV
Zone and did not exceed here the FrasnianlFamennian .... ,... .. "1"1,, ... , I .... ' ' ' ' ' ' ' ' ' ' . . , . . ... ''''''',~''
the known remnants of the carbonate p!8,UOirm per'slsted
and the fossil content of the limestone turbidites HlL'-'ll...·Q.I.::Ll!lJIJ:; basinal
OUIl1OlJpS were active at least to the Upper Zone.
A considerable of the carbonate is cOlnoJose:d of dolomites. The eOgelletlc dolomites are confined to the earliest phase of its The
r!('\II('\n .... ;t~.C' which reach the but are more common
the dolomitization process was M. Narkiewicz 1) for it
fJV"'-''''''V solutions.
Its
ref.!:arclea these dolomites as
THE PELAGIC CARBONA TE PLA TFORM
1"I,..""" ... ,."i'r of the shallow-marine carbonate I-'L~.UV"" and its transfonnation into a
M. and northern
to the Tournaisian.
The encroachment of a low-rate pelagic over the shallow-marine carbonates CornpJlere:a late in the when it invaded the
paJlae(}~c~ogTar>hY was dominated
carbonate two intra-shelf basins.
A thickness of the condensed limestones is with a thickness of the coeval basinal which are up to one thousand times thicker. The condensed 1"1"",,,,,,1,-.,,,,,.1"1 in two facies: crinoidal and The crinoidal
in the Lower Famennian. The V'-'~)"U.1U~JUU
in the
segregatlcm of biotic cornp()nents
the Famennian condensed delJ05ats 1981,
tenninated in the Tournaisian
czewski et in Near the northern IJHJ,LIU'Llll the condensed sequence is restricted to the Lower Famennian and then is V~A'Llvl:JI" basinal de[:loslts
1971,1981,
THE MIDDLE TO UPPER DEVONIAN INTRA-SHELF BASINS
The Middle to Devonian evolution of a palae()toIPO$~raIJhY in the area of the HeM
is a of intra-shelf basins them
carbonate ... I",f-+I"'\,..,....,. The two basins
extent and It makes a pel1symrnerncal " ' ' ' ... ·HU'']; facies
De~)osiltionalevolution of the Holy Cross Mts ... 481
distribution. The depth of the basins did not exceed several hundreds metres, but often was less, especially in the Middle Devonian. The lithology of basins-fill is dominated by and carbonate clastic rocks being exceptionally rare.
THE NORTHERN BASIN
The northern basinal area of the HeM was only the southernmost fragment of the broad basin, far to the north. The basinal setting appeared just after cessation of the Lower Devonian clastic It throughout the Devonian, interrupted
only basinward shift of more shallow and margin-
no1te'0.lorlthv eX2lffi1=lles are the Eifellan tong of the the Givetian of the Pokrzy-
wianka Beds and the Frasnian (Kostoml:oty Beds).
The Middle Devonian basin-fill is infonnally termed "a facies", since it consists of intercalated with variable limestones and marls Forma- tion, Skaly Formation, Nieczulice often contain abundant and diversified fossil assemblages, mostly benthonic, but nektonic fossils are also enc:ountered F-,VJllALLL.L"",IrlCIl.ldlng. The Swi~tomarz Formation is the stratigraphic unit within the basinal sequence, since it comprises fine clastics. J. Ktossowski (1985) demonstrated that sedimentological indicators point to their westward transportation.
In the Upper Givetian and Frasnian the basinal facies (Szyd16wek significantly shifted southward (G. Racki, 1985; G. Racki et al., 1985). Finally, late in the Early Famennian, they encroached over the of the isolated carbonate platform, succeeding the condensed cephalopod limestones. The Devonian basinal deposits mostly represent depositional settings to the Middle Devonian ones (M.
Narkiewicz, L 1983; H. Matyja, M. Narkiewicz, 1992, 1995). They
are less fauna. It consists of nektonic, planktonic
and oxygen Different and far more differen-
tiated fauna is included in the crinoidal resedimented from the central swell by debris flow (G. Biernat, M. ,szlulcze\lVs~:l.
In the eastern of the Kielce (Prucki, J ar1CZ.VCle.
cephalopod limestone are inserted within the basinal delpmats
H. Matyja, M. Narkiewicz, 1995). precisely correlate with rises of the sea
""''''''''''1"\1"",rt by 1. G. Johnson et al. The lowermost limestone is situated
at the FrasnianlFamennian boundary and is of the well-known KeHwasser- kalk.
The thickness of the Middle to Upper overlying Eifelian extension of the carbonate platform Wojciechowice Formation), probably exceeds 1000 m. It includes the which is up to roughly 300 m thick.
THE SOUTHERN BASIN
The appearance of the southern basin is closely related with an isolation of the central carbonate platform. The basinal deposition commenced in the Upper Givetian by drowning of a portion of the carbonate which attained its bank phase of The
basin in the but nevertheless it remained
was identified still at the southern border of the HeM
influenced de~)OSltlcm in the basin as a source of resedimented carbonate debris and as a which restricted water circulation. The carbonate turbidites are common in the Frasnian rI""",,,,,,,,t,, but the last distal ones occur in the Famennian. A
influenced biota in the basin (G. G.
feature of the evolution environments in the Famennian is their DrCIQ:n~SSJlnQ.
transformation from anaerobic to well ones, acc:onlpalOlf:d up.
Near the end of the Famennian the basin and the aalaC(~nt central swell became almost of
Kowala which cOJnDletc~d
THE LOWER CARBONIFEROUS BASIN
The Lower Carboniferous are soft and
were nowhere encountered in have been eroded. However, in the Kielce
fh1",n,H'.h drill record. The correlation of
retlec:tm,g a basins - swen thickness distribution and diachronism of facies boundaries indicates that the swen affected the
pattern until the Visean.
Over the carbonate the Carboniferous is known from very limited localities. it has been found that the condensed limestones of the carbonate include the Lower and Middle Tournaisian at its summit
H. M. Szulczewski et
existence of the low-rate det)Oslt1c1n palae()nt()lOgICaJ content of the UIU.J':'Ul£Ul
Elsewhere this stnl.tlgrap'hlc norldelPos!twiflal gap.
The Famennian and Lower Carboniferous succession evidences
toumd'~nrlg of the carbonate The facies of the succec:OHlg
mcrealSU:lQ: rate of accumulation. The
""T·1"'''' .... +'',,;- C()mple~x of .... ,,,, ... .,'1'-.
Depositional evolution of the Holy Cross Mts ... 483
this complex indicate its deposition in a wen aerated environment situated at the swell-to- basin transition (M. Szu1czewski et at.. in press).
The drowning was completed in the Visean with onset of deposition of black siliceous shales (Zar~by Formation). They are here attributed to the Lower and Middle Visean (M.
Szu1czewski et
at.,
in press). The black shales are laminated and organic rich. They contain abundant radiolarians and subordinate sponge spicules. Their features point to an anoxic depositional environment at a depth of several hundred metres.The lithologies typifying the two above described units. which follow the condensed sequence over the buried carbonate platform, continue beyond it to the former basinal area, but their thickness increases conspicuously in this direction. The alternating limestones and shales are only about 3.5 m thick over the platform but outside it a thickness of the corresponding Radlin Beds attains up to 20 m (H. Zakowa, 1981). The black shales of the
Zar~by Formation are respectively from 25 (or possibly up to 60 m) to about 250 m thick (H. Zakowa, 1981). Moreover. beyond the platform at least the lowest 90 m of the black shales belong still to the Tournaisian (H. Zakowa, 1981; H. Zakowa, M. Paszkowski, 1989), while above the platform their base is situated within the Visean.
The Lower and Middle Visean was a period of the most unificated and the deepest depositional environments in the Upper Palaeozoic history of the HCM. The accumulated deposits are hemipelagic noncarbonate clays. They are laterally differentiated only into aforementioned more siliceous facies (Zar~by Formation), akin to Kiesellschiefer, and the nonsiliceous one (former Garno Beds, included in Lech6wek Formation by H. Zakowa and Z. Migaszewski. 1995). Although their depositional setting remind of "bathyal lull".
governing penecontemporaneously many regions in the Variscan realm, their accumulation rate was relatively high. since the G6rno Beds attain 75 to more than 400 m in thickness (H. Zakowa, 1981).
Appreciably contributing to the accumulation of the all above described Carboniferous units were tephra deposits (H. iakowa et aI., 1984; Z. Migaszewski, 1995; R. Chlebowski, 1995). They appear as early as in the uppennost Famennian. Over the swell peaks of volcanic activity coincide with several boundaries between the units reflecting successive phases of its drowning. It confirms that the foundering was significantly affected by extensional tectonics (M. Szulczewski et al., in press).
Conspicuous turnover in the depositional regime is marked within the Upper Visean by onset of siliciclastics upon hemipelagic deposits of the Zar~by Formation and G6rno Beds.
The clastic deposits are some hundred metres thick, generally fine-grained and contain more clay and mudstones than sandstone intercalations. They belong to the Lech6wek Forma- tion, the Gulaczow Member including (H. Zakowa, Z. Migaszewski, 1995), the latter more sandy and containing thicker sandstone intercalations than the fonner. They still wait for sedimentological analysis.
This transformation of depositional regime was heralded by an abrupt deposition of the coarse-grained lenticular carbonate bodies (GaJ~zice Debrite Member ofH. Zakowa and Z.
Migaszewski. 1995). They Occur in the southwestern corner of the HCM, close to the Middle/Upper Visean boundary. According to Z. Berka and
s.
Skompski (1988) they are carbonate gravity flow deposits. They were deposited as submarine fans, situated in a deep lower-slope environment ofZar~by Formation. Their Frasnian to Visean debris derjve fromanother, hypothetic, more long-lived carbonate platform. Z. Belka et ai. (in press) suppose . that it was situated about 10 km to the south and name it the Nida Platform.
The source of the Upper Visean siHclclastic deposits seems, on the other hand, to be situated to the north or north-west of the HCM. It was probably created by the approaching front of the Variscan orogeny. The Palaeozoic succession of the HCM was folded during this orogeny. The youngest folded strata belong to the Upper Visean, and the oldest unconformably overlying them are the Permian. Hence, a broad and significant time-span of geological history of the HeM is devoid of its direct stratigraphic record.
Acknowledgments. Assistance in preparation of illustration, kindly offered by Michal Zywiecki is acknowledged with gratitude.
Instytut Geologii Podstawowej Uniwersytetll Warszawskiego Warszawa, aJ. Zwirki i Wigury 93 Received: 17.lD.1995
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EWOLUCJA DEPOZYCJI W W DEWONIE I KARBONlE-
PRZEGL~DPROBLEMATYKI
Streszczen e
Pr~dki przyrost wiedzy i karbonie podjccia pr6by przeglfjdu
wa:zni,ejs:lyc:h publikacji, si~ fla obraz g16wnych zjawisk i problem6w rozwoju facjalnego w tym prz.ed:1:iale stratygraficznym, artykut, lemu Do!;wieccmv
wersja opracowarlin przedstawlonego nn konferencji mjt~dzvn:lfo,dO\l\Ie,!O
sie w Kielcach w 1994
DewDn i do loy karbon G6r podporzq,dkowany
dtugotrwalej trarlsgc'esJl kaledotiskq i UJ~!nJ>:!,i"'V;,~Ir~
Dolny dewon jest wyksztatcony gt6wnie jake sukcesja klastyczna. W jej srodowiska l<1dowe i morskie, ai po ostateczoll transgresje morsh w emsie. Wzor zr6i.nlcowania Jej mhl7,szosci, zapisu wyrazistll, ilustracja odmieonosci rezimu depozy-
chronostratygraficznego seClyn1enltac:ji poszczeg61nych formacji wnr3\11/dzie niajqcych deklarowane zapatrywania. Stl1d
dertOZ'\lcH i regionalnego znaczenia. zlepienca mit~dzianlog;6rskiego.
M. Tamowskiej, Ze facje morskie w g6mej
tacji klaslycznej i WOfO\il/ac[zi!
Rychle splycenie i unifikacja srodowisk depozycjj zapoczatkowaty z kolei dJugotrwaiy rozw6j ptytkowodnej p}altt-ormv w~glanowej. skamieniaJosci i zjawisk fizycznych spowodowalo, jej aspekty
str:atygraltlcznj~, s(~d}'rmEmt(}[ogtczne i od lat na sobie najwii;?cej uwagi badaczy. G16w- nymi znamionami ewolucji platformy by to obszaru, wuost zr6i:nicowania reliefu
i rosnqce znaczenie budowli organicznych. Z trzech dominacj!l
wok6Jplywowych ub6stwem budowli organicznych, !l kolejne odpowiadajll fuie i rafowej z renskiego. W fazie rafowej platfonna osiqgn~la zloiony ukfad facji, OOI)QI;vladalacy systemowi depozycyjnemu izolowanej platfonny wt;glanowej, rafami i piyciznami
M. Narkiewicza, dyminski kompleks rafowy G. Rackiego). Stromatoporoidowo~koralowcowy zesp6t organizmow zanikl przed koncem franu, ale oznaki istnienia plytkowodnej platformy pojawiaj4 si~ jeszcze dlugo w famenie.
Na p61nocy i poludniu z ptytkowodn::t platform::t s::tsiadowaly baseny sr6dszelfowe. BaseD p61nocny si~gal
daleko poza G6ry Swietokrzyskie i wyodrebnH si<t jui: u schylku wczesnego dewonu. Powstanie wezszego, poludniowego basenu jest r6wnoznaczne z izolacj~ platformy w jej stadium rafowym. Centralnie usyluowana platfonna wplywafa na sedymentacje w basenaeh jako zr6dlo resedymentowanego materialu oraz jako pr6g ograniczajqcy cyrkulacje.
Czesc platformy weglanowej zatopiona w g6mym dewonie przeksztalcila sie w peJagiczDq platforme
w~glanow~. Stanowi& ja skondensowane wapienie glowonogowe i krynoidowe, si~gaj~ce !okalnie nawet srod- kowego tumeju. Spoczywajf.l one czesto na weglanach platformy niezgodnie i wnikajq w nia w fonnie roznowie- kowych iyl neptunicznych.
W dolnym karbonie wz6r facjalny ulega uproszczeniu. Sukcesja stratygraficzna zwykle rozpoczyna sie naprzemianlegtymi wapieniami i tupkami. a przykrywaj~ je ezarne lupki krzemionkowe oraz ilaste. Wptyw pogrqionej platformy weglanowej WYraZa sie jui tylko w r6znicach mi<\Zszosci tych formacji i w diachronizmie dzielllCej je granicy. Zasadniczy zwrot w reiimie sedymenlacyjnym nast!l-pil w g6rnym wizenie wraz z pojawie- niem si~ kompleksu siliciklastycznego. zamykajqcego zachowanq. sukcesje karbonskq. Poprzedzi!a go lokalna depozyeja soczewek wapiennych. uwaianych obecnie za stoZki podmorskie, utworzone z materialu grawitacyjnie przemieszczonego z dluzej tlWajqCej, hipotetycznej platformy wr:glanowej, poloionej na poludnie od Gor Swir:tokrzyskich. Zdarzenia te wi1i2e sie jui z aktywnosciq tektoniczoq, ktora wkr6tce przyniosla emersje i wywolala niezgodnosc waryscyjskq.
