Or do vi cian through ear li est De vo nian de vel op ment of the Holy Cross Mts. (Po land):
con straints from sub si dence anal y sis and ther mal ma tu rity data
Marek NARKIEWICZ
Narkiewicz M. (2002) — Or do vi cian through ear li est De vo nian de vel op ment of the Holy Cross Mts. (Po land): con straints from sub si - dence anal y sis and ther mal ma tu rity data. Geol. Quart., 46 (3): 255–266. Warszawa.
The Łysogóry Block (ŁB) ex posed in the north ern Holy Cross Mts. (HCMts.) re veals sub si dence and ther mal de vel op ment con sis tent with the pat tern ob served in ad join ing East Eu ro pean Craton (EEC) ar eas. This ev i dence, in ad di tion to pre vi ously re ported sim i lar i ties in sed i men ta tion and deep crustal struc ture, con tra dicts the Pożaryski’s hy poth e sis that the Łysogóry Block rep re sents a terrane within the Cal edo nian orogen. This area is here in ter preted as the part of a Late Si lu rian foredeep ba sin which de vel oped on the Baltica mar gin in re - sponse to ter mi nal phases of col li sion with East ern Avalonia. The de vel op ment of the con tin u ous Late Si lu rian foredeep ba sin along the EEC mar gin from the Peri-Tornquist Ba sin in the north-west to the pres ent north ern HCMts. im plies that the North Ger man-Polish Caledonides orogen had its NE con tin u a tion near the pres ent Holy Cross area. The south ern HCMts. com prise the north ern mar gin of the Małopolska Mas sif (MM). The Or do vi cian-Silurian sub si dence de vel op ment of this area, its ther mal his tory and crustal struc ture point to a sta ble cratonic set ting. Ex isting sim i lar i ties in sed i men tary suc ces sion (mostly Or do vi cian and Lower Si lu rian) as well as clearly Bal tic palaeobiogeographic af fin i ties in di cate a close spa tial con nec tion be tween the MM and Baltica dur ing the ana lysed time interval. The jux ta po si tion of the MM against the ŁB area can be ex plained as sum ing that the MM is a part of Baltica de tached from its mar gin due to right-lateral strike-slip af ter late Lud low and be fore Emsian time.
Marek Narkiewicz, Pol ish Geo log i cal In sti tute, Rakowiecka 4, PL-00-975 Warszawa, Po land; e-mail: mnar@pgi.waw.pl (re ceived:
April 17, 2002; ac cepted: May 7, 2002).
Key words: Trans-European Su ture Zone, Holy Cross Moun tains, Early Palaeozoic, tec tonic sub si dence, ther mal his tory, ter ranes.
INTRODUCTION
The Palaeozoic de pos its of the Holy Cross Moun tains (HCMts.) in south-cen tral Po land, al though areally lim ited, are nev er the less im por tant for the re gional ge ol ogy of Cen tral Eu - rope. These de pos its re cord the evo lu tion of a ma jor tec tonic zone — the Trans-Eu ro pean Su ture Zone (TESZ — Berthelsen, 1993; Pha raoh et al., 1997; Pha raoh, 1999). In par - tic u lar, they are a sen si tive re corder of Early Palaeozoic phases of con ti nen tal ac cre tion along the pres ent south west ern mar gin of the Baltica palaeocontinent (pres ent East Eu ro pean Craton
— EEC, Fig. 1). The course of ac cre tion still raises much con - tro versy as to the re gional scale and de tailed sce nario of events (Pożaryski, 1990; Dadlez et al., 1994; Pha raoh, 1999; Belka et al., 2000).
The key prob lem in this con text is an in ter pre ta tion of geo - log i cal struc ture, evo lu tion and mu tual re la tion ship of sev eral crustal blocks, two of which — the Łysogóry Block and Małopolska Mas sif — out crop in the Holy Cross Mts. The ob - jec tive of this pa per is the Early Palaeozoic evo lu tion of these
units and their re la tion ship to Baltica/EEC in the light of tec - tonic sub si dence anal y sis of the Or do vi cian to Lower De vo - nian, and ther mal ma tu rity lev els of the Lower Palaeozoic. One of the main aims of the study is to test if the pos si ble terrane na - ture or col lage pat tern of crustal blocks is to any de gree re - flected in their sub si dence pat terns and ther mal sig na tures.
REGIONAL BACKGROUND
The Palaeozoic out crops of the Holy Cross Mts. ex tend across the bound ary be tween two ma jor re gional units (Fig. 1;
i.a. Pożaryski, 1990; Dadlez et al., 1994; Belka et al., 2000).
The north ern part com prises a south ern mar gin of the Łysogóry Block (ŁB) named af ter the Łysogóry Range in the HCMts. A north ern part of the Małopolska Mas sif (MM) is ex posed in the south ern HCMts. These units are dis sim i lar in re spect to their geo phys i cal char ac ter is tics, in clud ing in ter preted crustal thick - ness (see re view in Dadlez, 2001), and also show dif fer ences in their Palaeozoic sed i men tary de vel op ment (see e.g. Szulczew -
ski, 1977, 1996; Belka et al., 2000). The ŁB ad joins the north- eastern flank of the Late De vo nian-Car bon if er ous Lublin Trough, which is lo cated in the East Eu ro pean cratonic do main (Żelichowski and Kozłowski, 1983). The pres ent bound ary runs along the ma jor Kazimierz-Ursynów Fault Zone (Pożaryski and Tomczyk, 1993; Dadlez, 2001) dis play ing a strong lat est Car - bon if er ous transpressional over print. In turn, the Małopolska Mas sif is bor dered by the Up per Silesian Block along the Kraków-Lubliniec Fault Zone in the south-west (Buła et al., 1997). Most au thors agree that the de scribed pat tern of par tic u lar blocks emerged gen er ally dur ing pre-Variscan times and has not un der gone ma jor ro ta tions or trans la tions since the Early De vo - nian (Pożaryski et al., 1992; Dadlez et al., 1994; Znosko, 1996) al though opin ions were also ex pressed on the dom i nant role of Variscan tec ton ics (Stupnicka, 1992; Lewandowski, 1993).
Ac cord ing to some au thors the MM is in fact com posed of sev eral sub or di nate units of dif fer ent geo log i cal de vel op ment.
E.g. Mizerski (1995) dis tin guished the north ern Kielce Block and south ern Miechów-Rzeszów Block, while Belka et al.
(2000) de fine the east ern part of MM as the San Block, whereas their Łysogóry Block may be com posed of smaller units, po - ten tially sep a rate ter ranes. Con fir ma tion of these con cepts, how ever, re quires fur ther stud ies en abling better geo log i cal and geo phys i cal res o lu tion.
The bound ary be tween the MM and the ŁB is drawn along the Holy Cross Fault (HCF) gen er ally cor re spond ing to a
crustal frac ture zone (Guterch et al., 1976, 1986; Pożaryski and Tomczyk, 1993; Dadlez, 2001). This fault shows a strong Variscan over print re lated to transpression (Pożaryski et al., 1992). While in the east ern Holy Cross Mts. the bound ary be - tween both blocks seems in deed to fol low pre cisely the HCF, in its west ern part I con sider that it runs far ther to the south, along the north ern limb of the Dyminy Anticline (Fig. 2). Such a course is sug gested by the shift in strike of the Palaeozoic struc - tures to nearly E–W in the south west ern HCMts. It is also re - flected in a sep a rate po si tion of the Kielce area in the De vo nian palaeogeographic pat tern (the “Kostomłoty tran si tional zone”
— Racki, 1993). The more south erly course of this bound ary may be also ex pressed in the later (in her ited) trend of the Włoszczowa-Ryko szyn- Karczówka Fault Zone men tioned by Pożaryski (1974, p. 338). The re sults of sedimentological stud - ies by Malec (2001) in di cate the Łysogóry prov e nance of clasts in greywackes and con glom er ates from the top of the Si lu - rian-low er most De vo nian se quence in the Kielce area, south of the HCF. In ad di tion, the re sults of the pres ent stud ies of the Lower Palaeozoic (see be low) are in agree ment with the cor - rected course of the MM/ŁB bound ary in the west ern HCMts.
as shown in Fig ure 2.
PREVIOUS STUDIES
Un til the 1980”s, dis cus sion on the tec ton ics of the Holy Cross Mts. fo cused on whether Palaeozoic and/or Pro tero zoic orogens were pres ent, in par tic u lar the Cal edo nian and Variscan ones, ei ther in the en tire re gion or only in its south ern ver sus north ern parts (see sum ma ries in Tomczyk, 1974; Da dlez et al., 1994). In the mean time, how ever, it be came clear that the Palaeozoic suc ces sions of the Holy Cross Mts. lack at trib utes of a
“typ i cal” collisional orogenic belt, such as con sid er able crustal short en ing and char ac ter is tic in ter nal sedimenary-stru ctural ar chi - tec tures. In par tic u lar, Szulczewski (1977) con vinc ingly dem on - strated the epicontinental char ac ter of the Palae ozoic de po si tion in the whole Holy Cross Mts. area. At pres ent, the re main ing pro po - nents of the “orogenic ap proach” dis cuss mainly the rel a tive im - por tance of suc ces sive stages of tec tonic de for ma tion (cf. e.g.
Stupnicka, 1992; Mizerski, 1995; Znosko, 1996).
The turn ing point in pre vi ous stud ies was the pa per by Pożaryski (1990) who in ter preted the Holy Cross Mts. as a frag - ment of the Cal edo nian strike-slip (left-lateral) orogen com posed of ter ranes, in clud ing the Łysogóry terrane and the terrane of Małopolska Mas sif. This mobilistic con cept was pre ceded by the hy poth e sis by Brochwicz et al. (1981) on a con ti nen tal-scale, left-lateral trans la tion along the SW-edge of the East Eu ro pean Plat form dur ing the Early Palaeozoic. In this con text one should also men tion the palaeomagnetic study by Lewandowski (1987) who in ter preted large-scale dis place ment of the Małopolska Mas - sif rel a tive to EEC, in the Early Palaeozoic.
The terrane con cept by Pożaryski (1990, see also Pożaryski et al., 1992; Pożaryski and Tomczyk, 1993) was criti cised by Dadlez et al. (1994). These au thors raised meth od olog i cal ob jec - tions to the de fin ing of ex otic ter ranes by Pożaryski (1990) and cited strati graphi cal, palaeomagnetic and palaeobiogeo graphical ev i dence ques tion ing the va lid ity of par tic u lar ter ranes, es pe -
E A S T E U R O P E A N C R A T O N
UKR AINIAN S HIE LD
HOLY CROS S MTS . BO HE MIAN
MAS S IF
MOES IAN P LATFORM C A R
P AT H
IA N
S BALTIC
S HIE LD
CDF STZ
MBH
ŁB MM
- GERMAN-PO LISH CALEDON
IDES
US B
0 500 km DO
P ODLAS IE DEP RES S ION
LUB TROUGLINH BALTIC BASIN N
V A R I S C I D E S
Fig. 1. Lo ca tion of the study area against the sim pli fied ge ol ogy of cen - tral Eu rope (partly af ter Pha raoh et al., 1997, fig. 1)
STZ — Sorgenfrei-Tornquist Zone, CDF — Cal edo nian De for ma tions Front, MBH — Mazury-Belarussian High, ŁB — Łysogóry Block, MM — Małopolska Mas sif, USB — Up per Silesian Block, DO — Dobrogea Orogen
cially the Łysogóry terrane. Ac cord ing to these au thors the Łysogóry formed part of the pas sive mar gin of the EEC (miogeocline) whereas the Małopolska Block is merely a pos si - ble prox i mal terrane trans lated dextrally along the EEC (i.e.
Baltica) mar gin not later than in the ear li est De vo nian.
In spite of the crit i cism ex pressed by Dadlez et al. (1994) other au thors fol lowed Pożaryski’s con cepts by ap ply ing his model ei ther di rectly (Franke, 1995; Unrug et al., 1999) or with some mod i fi ca tions in clud ing a Gondwanan prov e nance of ter - ranes and dif fer ent times of their ac cre tion (Valverde-Vaquero et al., 2000; Belka et al., 2000). The last two pa pers re port new data on de tri tal ma te rial prov e nance based on zir cons and mus co vite dat ing, as well as provide a re view and dis cus sion of pub lished biogeographical data on dif fer ent fos sil groups. In turn, new palaeomagnetic data was pre sented by Nawrocki (2000) ac cord - ing to whom “...tec tonic move ments and ac cre tion of blocks along the SW edge of Baltica must have oc curred be fore the lat - est Si lu rian...”and thus con trary to Lewandowski’s (1993) con - cept of a right-lateral Late Palaeozoic trans la tion of the MM.
In sum mary, the terrane hy poth e sis by Pożaryski (1990) ap - peared an im por tant al ter na tive for a “clas si cal” collisional orog eny model in the area de scribed. How ever, the po ten tial ter ranes still lack con vinc ing and com pre hen sive ex pla na tion and their bound aries are not pre cisely de fined. There is also a lack of a con sis tent sce nario ex plain ing the mu tual spa tial and tem po ral re la tion ship of blocks/ter ranes and the EEC as well as their strati graphi cal, sed i men tary, biogeographical, tec tonic (sub si dence de vel op ment) and ther mal at trib utes.
SUBSIDENCE ANALYSIS
The pres ent sub si dence anal y sis was per formed us ing a backstripping pro ce dure which en ables ex trac tion of a tec tonic
com po nent from to tal sub si dence (e.g. Angevine et al., 1990;
Al len and Al len, 1990). The cal cu la tions were per formed us ing the com mer cially avail able BasinMod 1-D soft ware. Harland’s et al. (1989) scale was used as a time ref er ence and Sclater and Chris tie’s (1980) al go rithms were ap plied in decompaction pro ce dures. In or der to test the sen si tiv ity of the re sult to dif fer - ent ver sions of the geo log i cal col umn the backstripping was re - cal cu lated us ing the more re cent time scale (Gradstein and Ogg, 1996). How ever, the dif fer ences be tween the re sults ap - peared in sig nif i cant for the con clu sions of this study.
STRATIGRAPHY
The stud ied suc ces sions com prise Or do vi cian to Up per Si - lu rian-lowermost De vo nian de pos its un con form ably over ly ing var i ous Cam brian rocks (Dzik and Pisera, 1994;
Kowalczewski, 1994). In the south, the up per Tremadoc or Arenig de pos its rest on the Lower to Mid dle Cam brian with a dis tinct an gu lar disconformity. In the north ern re gion the un - con formity is less con spic u ous and the strati graphic gap en - com passes prob a bly only the up per part of the Tremadoc.
The sed i men tary suc ces sion is gen er ally sim i lar in both the stud ied ar eas of the Holy Cross Mts., how ever it con sid er ably dif fers in thick ness, rang ing from ca. 300 metres in the south to 1000–1500 metres or per haps even 2000 metres in the north (Fig. 3). At its base it is de vel oped as thin transgressive ma rine clastics (mostly Arenig) over lain by cal car e ous or shaly-cal car - e ous de pos its rep re sent ing con densed Mid dle Or do vi cian (Llanvirn to Caradoc) car bon ates (Dzik and Pisera, 1994).
They are suc ceeded by dark grap to lit ic shales and/or mudstones com pris ing mostly the Up per Or do vi cian (Ashgill) to the mid dle part of the Si lu rian (lower Lud low). In the south, the up per most part (up per Lud low) con sists of var i ous ma rine clastics, mostly siltstones and greywackes with a con sid er able
Vistula Post-Permian deposits
Lower Palaeozoic
Devonian
Carboniferous
Permian
Holy Cross Fault
SANDOMIERZ KIELCE
ŁYS OGÓRY
ZA
a re a s of de ta ile d s ubs ide nce s tudie s KA
BS
10 km
Ma łopols ka Ma s s if/
Łys ogóry Block bounda ry DA
Fig. 2. Sim plified geo log i cal map of the Holy Cross Moun tains with a lo ca tion of the ar eas/sec tions whose Or do vi cian-Early De vo nian sub si dence is ana lysed
ZA — Zbrza Anticline, BS — Bardo Syncline, DA — Dyminy Anticline, KA — Kielce area
volcaniclastic com po nent, pass ing up wards into sand stones and mudstones in ter preted by Przybyłowicz and Stupnicka (1989) as shal low ma rine, prob a bly nearshore fa cies.
Ter mi na tion of the Or do vi cian-Silurian ba sin de vel op ment is re lated to Late Cal edo nian tec tonic move ments (e.g.
Pożaryski, 1990; Dadlez et al., 1994). In the south ern re gion and over the en tire MM area they were man i fested in struc tural in ver sion and re lated compressional or transpressional de for - ma tions, up lift and strong ero sion. Late Cal edo nian disconformity is over lain by terrigenous clastics as cribed ge - nerally to the Emsian (e.g. Szulczewski, 1995).
The up per part of the Si lu rian in the north ern re gion is con sid - er ably thicker and more com plete, com pris ing the up per most part of the sys tem (Přidoli) with a tran si tion to the low er most De vo - nian de pos its. Al though its de tailed stra tig ra phy is still de bat able, a gen eral sed i men tary suc ces sion seems to be es tab lished (cf.
Malec, 1993b, 2001; Kowalczewski et al., 1998). Graptoli tic shales are over lain by rhyth mi cally bed ded shales and graded beds of graywacke siltstones and sand stones be long ing most prob a bly to the up per Lud low. These sed i ments are in ter preted by Malec (1993a, 2001) as deeper-water flysch de pos its. Based on pre lim i - nary stud ies of cur rent mark di rec tions Malec in ter prets source ar - eas for the clastics as be ing lo cated in the south-west or west, out - side the Małopolska Mas sif area (Malec, 2001).
The graywackes pass up wards into more shaly de pos its with sub or di nate sandy and/or limy interbeds and with an open ma rine fauna, also in ter preted as a deeper-water flysch. The uppermost part of the suc ces sion is com posed, in a clearly shallowing-upwards fash ion, of coarser-grained, sandy to con - glom er atic de pos its. Kowalczewski et al. (1998) in ter pret the lat ter as braid delta, braid plain to al lu vial fan fa cies, ap par ently
re flect ing re gres sion in the ba sin prior to the up lift. The age of these de pos its is dis put able al though re cent palynostratigraphic in ves ti ga tions point to the lat est Přidoli-earliest Lochkovian (Turnau in: Kowalczewski et al., 1998). It is, how ever, prob a - ble that they may be diachronous, rang ing higher into the Lochkovian (cf. Malec, 1993b; Szulczewski, 1995). They are over lain — con form ably or with a small an gu lar un con formity
— by thick al lu vial clastics start ing a new basinal cy cle and as - cribed to the Siegenian (Pragian)-Emsian.
The backstripping anal y sis em braced four syn thetic strati - graphic sec tions: two from the south ern re gion (Zbrza Anticline and Bardo Syncline) and two from the north ern one (north-west of Kielce, and the Łysogóry area di rectly to the north of the HCF; Fig. 2). The Zbrza sec tion was com piled from Deczkowski and Tomczyk (1969). The Bardo sec tion is based on de scrip tions by Bednarczyk (1981), Tomczykowa and Tomczyk (1981), Dzik and Pisera (1994) and Kowalczewski (1994). Two vari ants of the backstripping re - sults re flect dif fer ent es ti mates of the thick ness and stra tig ra phy of the Up per Si lu rian greywackes by Romanek and Rup (1989, vari ant A in Fig. 3) and Stupnicka et al. (1991, vari ant B).
The lower part of the Kielce sec tion was com piled us ing data from Dzik and Pisera (1994) and Kowalczewski (1994).
Again, two vari ants rep re sent dif fer ent thick ness es ti mates of the Up per Si lu rian, those ac cord ing to Malec (1993b, vari ant A) and those of Stupnicka (1995, vari ant B). The lat ter vari ant also as sumed that the Late Si lu rian flysch sed i men ta tion ended be fore the Přidoli whereas in the for mer it was as cribed to the late Lud low and Přidoli. The Łysogóry se quence is based on sev eral sec tions de scribed by Bednarczyk (1981), Dzik and Pisera (1994) and Kowalczewski (1994). Vari ants A and B re - flect dif fer ent thick ness es ti mates of the greywacke and clayey de pos its of the Up per Si lu rian and low er most De vo nian by Tomczykowa and Tomczyk (1981) and Kowalczewski (1994) ver sus Jurewicz and Mizerski (1987).
It should be stressed that the strati graphic data used for the pres ent study are of vari able qual ity, partly due to poor ex po - sures and frag men tary bore hole sec tions. Lo cally (Fig. 4) it was nec es sary to ex trap o late data from neigh bour ing sec tions/ar eas.
More over, the chronostratigraphy was partly based on lo cal sub - di vi sions, and the cor re la tion with the stan dard ep ochs or stages is ar bi trary and may be im pre cise. This re fers mainly to the Up - per Or do vi cian and Up per Si lu rian units. Al though the poorly-con strained strati graphic data is con sid ered to be the main source of er ror in backstripping cal cu la tions it is nev er the - less as sumed here that the re sults do re flect gen eral sub si dence pat terns on a re gional scale. Fur ther re fine ments in stra tig ra phy will most prob a bly change the de tails of the tec tonic sub si dence de vel op ment but the over all trends should re main.
PALAEOBATHYMETRY AND EUSTASY
There are only scarce pub lished in ter pre ta tions of the ab so - lute palaeowaterdepths of ana lysed de pos its. In most cases in - ter pre ta tions are purely qual i ta tive and re fer mainly to nearshore ma rine or con ti nen tal de pos its of the low er most and up per most parts of the stud ied suc ces sion (as de scribed above).
Ob vi ously, in the lat ter cases palaeobathymetric cor rec tions are not im por tant for re sults of the anal y sis. The main prob lem in
? ?
? lime s tone
gre ywa cke
muds tone
s ha le qua rtz s a nds tone
S OUTHERN HOLY CROS S MTS .
NORTHERN HOLY CROS S MTS .
DEVONIAN (EMS IAN)
S ILURIAN
ORDOVICIAN LOWER-MIDLLE CAMBRIAN
UP P ER CAMBRIAN LOCHKOVIAN
P RAGIAN
0 m 100 200 300 400 500
Fig. 3. Com par i son of stra tig ra phy and gen eral li thol ogy of the south ern and north ern part of the Holy Cross Mts.; the sec tions are gen er al ised us -
ing data com piled from var i ous au thors cited in the text
that re spect is the palaeobathymetry of grap to lit ic shales (Or do - vi cian to lower part of Si lu rian) and siliciclastic de pos its of the up per part of the Si lu rian. The widely ac cepted epicontinental char ac ter of sed i men ta tion of these de pos its (Szulczewski, 1977; Dadlez et al., 1994) would con strain the max i mum waterdepths in the Or do vi cian to Early Si lu rian to a few hun - dreds of metres. The min i mum palaeobathymetry of the dark anoxic shales can be es ti mated at ca. 100 me ters cor re spond ing to the com monly as sumed depth to ox y gen-minimum layer in epicontinental bas ins (Byers, 1977; Stoakes, 1980). The up per part of the greywackes in the Kielce sec tion is in ter preted by Malec (2001) as a deeper-water flysch fa cies which would place it in waterdepths of the or der of at least sev eral hun dred metres. The over ly ing de pos its rep re sent a shallowing-upward se quence with waterdepths de creas ing most prob a bly to shal - low subtidal, pass ing to nearshore coarser clastic fa cies. Ac - cord ing to Przybyłowicz and Stupnicka (1989) the up per most Si lu rian in the south ern HCMts. was de pos ited in a shal - low-water nearshore ma rine en vi ron ment.
The im pact of eustatic changes on the sed i men ta tion of these de pos its was con sid ered only oc ca sion ally (e.g. Dzik and Pisera, 1994). For the pur poses of the pres ent pa per only a qual i ta tive sce nario of pos si ble global sealevel changes will be briefly dis - cussed, based on the re cent in ter pre ta tions by Barnes et al.
(1996) for the Or do vi cian and Kaljo et al. (1996) for the Si lu rian.
Ac cord ing to these pa pers, the on set of the Or do vi cian is marked by a global highstand ter mi nated by a eustatic sealevel drop in the late Arenig fol lowed by a lowstand in the Llanvirn.
The lat ter events are prob a bly re spon si ble for the oc cur rence of a con sid er able sed i men tary gap at the Arenig/Llanvirn bound - ary in the Mójcza sec tion (Dzik and Pisera, 1994), and, prob a - bly, also for the gen eral pres ence of gaps ques tion ably at trib - uted by Tomczyk (1974) to the tec tonic “Łysogóry phase”. The Late Or do vi cian highstand, es ti mated by Barnes et al. (1996) to be among the high est sealevels in the Phanerozoic, was punc tu - ated by a short-term eustatic min i mum re lated to the lat est Or - do vi cian (Hirnantian) gla ci ation (see also Dzik and Pisera, 1994, for the dis cus sion of this event in the con text of the Mójcza sec tion). The lat ter event is most prob a bly re spon si ble for the or i gin of the wide spread Or do vi cian/Si lu rian bound ary gap re garded by Tomczyk (1974) as ev i dence of the “Taconian phase”. Ac cord ing to Kaljo et al. (1996), the global sealevel had been sys tem at i cally ris ing since the ear li est Si lu rian with the eustatic max i mum at tained in the late Llandovery and early Wen lock. Sealevel started to drop in the late Wen lock and the max i mum lowstand is placed near the Gorstian/Ludfordian bound ary (Lud low) and in the Přidoli.
RESULTS AND INTERPRETATION
Fig ure 4 il lus trates con sid er able dif fer ences in the course and mag ni tude of tec tonic sub si dence in the two in ves ti gated ar eas of the HCMts. Both sec tions rep re sent ing the Łysogóry Block re veal con vex curves with an ini tial stage of mi nor Or do - vi cian to ear li est Si lu rian sub si dence fol lowed by an ac cel er a - tion start ing in the Wen lock (Łysogóry) or mid-Llandovery (Kielce). In both sec tions a pe riod of par tic u larly ac cel er ated sub si dence com prises the late Lud low, i.e. the time when
deeper-wa ter flysch fa cies de vel oped (Fig. 4). Such a sce nario is typ i cal for foredeep set tings in front of a thrust belt caus ing flex ural bend ing of a lithospheric plate mar gin (e.g. Angevine et al., 1990). A sim i lar in ter pre ta tion was adopted for com pa ra - ble Early Palaeozoic sub si dence his to ries of the Welsh Ba sin and Lake Dis trict Ba sin (King, 1994), Brabant Mas sif (Van Grootel et al., 1997), and the Peri-Tornquist Ba sin in north ern Po land (Poprawa et al., 1999).
The in clu sion of palaeobathymetric cor rec tions may even strengthen the above in ter pre ta tion since the Late Si lu rian flysch de po si tion may have oc curred in waterdepths ex ceed ing the range of 100–400 metres typ i cal of an outer con ti nen tal shelf. The lat ter set ting may be as cribed to the un der ly ing grap - to lit ic shales. It should be stressed that the depositional sys tems in ter preted for the Up per Si lu rian flysch sed i ments (Malec, 2000, 2001) are com pat i ble with the foredeep ba sin model. In the ex am ple de scribed the hy po thet i cal orogenic load could have been sit u ated south-west of the pres ent ŁB. This is in di - cated by both gen eral re gional con text (see be low — Dis cus - sion) and the data on sed i ment-transport di rec tions in the flysch suc ces sion (Malec, 2000, 2001).
In con trast to above de scribed sec tions, both the sec tions rep re sen ta tive for the north ern mar gin of the Małopolska Mas - sif dis play clearly lower and more uni form rates of tec tonic sub si dence. In the case of the Bardo sec tion, vari ant A cal cu la - tions give re sults qual i ta tively sim i lar to the Łysogóry sec tions.
If this vari ant is in deed more re al is tic than vari ant B, it may be eas ily ex plained in terms of chang ing palaeowater-depth his - tory, as sum ing rather con ser va tive palaeobathymetry cor rec - tions (Fig. 5). The low and rel a tively uni form rates of tec tonic sub si dence are typ i cal of sta ble cratonic set tings (e.g. Angevine et al., 1990; Einsele, 1992). In the MM area, the on set of coarser clastic de po si tion may be re lated to an eustatic fall in the late Wen lock (Kaljo et al., 1996).
REGIONAL PATTERN OF THERMAL MATURITY
The data ana lysed in clude ther mal ma tu rity in di ces for 12 lo cal i ties (Fig. 6). Most of the data (9 lo cal i ties) were ini tially TAI val ues de ter mined for the Cam brian by Szczepanik (1997) and for the Si lu rian (sec tion near Kielce) by Malec (2000 and pers. comm.). Both val ues for the Or do vi cian were based on cono dont CAI in di ces (Mójcza — Belka, 1990; Pobroszyn — Katarzyna Narkiewicz, pers. comm.). In ad di tion, a sin gle Tmax
(Rock Eval) mea sure ment was ob tained for the Si lu rian from Prągowiec near Bardo. All the data are ex pressed in cono dont CAI units for the pur pose of com par i son (Fig. 6).
Al though the ana lysed da ta base is lim ited it is nev er the less pos si ble to draw some gen eral con clu sions re gard ing re gional trends in ma tu rity dis tri bu tion. Fig ure 6 shows a dis tinct pat tern of a low or ganic ma tu rity in the south, with the CAI 1–2 cor re - spond ing to im ma ture rocks and the oil win dow (Ep stein et al., 1977). The data for the north ern MM mar gin con trasts with the val ues of CAI 3–5 in di cat ing overmature rocks in the south ern part of the Łysogóry Block. This pat tern is in de pend ent of the age of the re spec tive sam ples and thus re flects a dif fer ent over - all ther mal ma tu rity of both re gions. More over, it seems sig nif i -
cant that closely sit u ated lo cal i ties on op po site sides of the bound ary be tween the Małopolska Mas sif and the Łysogóry Block dis play con trast ing ma tu rity val ues (Fig. 6).
In gen eral, the low ma tu rity level in the Lower Palaeozoic of the south ern HCMts. cor re sponds to a low ma tu rity of the De vo nian and Car bon if er ous rocks in that re gion (Belka, 1990). Ac cord ing to that au thor the pres ent ma tu rity was at - tained prob a bly dur ing the Late Car bon if er ous (op. cit.).
Marynowski (1999) dem on strated that a zone of in creased ma tu - rity in the De vo nian cor re lates with the west ern part of the HCF and may be at trib uted to an in creased heat flow along this tec - tonic line. On the other hand, the Lower Palaeozoic data does not re veal any marked ten dency to in creased val ues to wards the MM/ŁB bound ary. Also, it does not show any de creas ing re - gional trend to wards east. There fore, it is here con cluded that the dis tri bu tion of ma tu rity val ues in the Lower Palaeozoic strata is
re lated to the pre-Variscan ther mal his tory. It is as sumed that it re flects first-order dif fer ences in the Early Palaeozoic ther mal re - gime of the north ern part of the MM ver sus the ŁB.
The low ther mal re gime in the MM part of the HCMts. im - plies that the re gional ther mal field in this area was not af fected by Early Palaeozoic tec tonic and/or mag matic events, nei ther near the Cam brian/Or do vi cian bound ary nor in the Late Si lu - rian-Early De vo nian.
REGIONAL SIGNIFICANCE OF THE RESULTS — A DISCUSSION
The re sults given here dem on strate con trast ing pat terns of the Or do vi cian to ear li est De vo nian tec tonic sub si dence in south ern ver sus north ern parts of the Holy Cross Mts. These
Łys ogóry (A)
Łys ogóry (B)
Kielce (A)
Ba rdo S yncline (A)
Ba rdo S yncline (B)
Zbrza Anticline Kie lce (B)
400 440 420
480 460 520 500
TECTONIC SUBSIDENCE (m)
0
200
400
600
800
1000
Ma
CAMBRIAN ORDOVICIAN S ILURIAN DEVONIAN
TREMADOC ARENIG LLAN-
VIRN LO. CARADOC A. LY. WEN. LUDLOW LOCHKO-
VIAN P.
GREYWACKE DEP OS ITION
SOUTHERN HCMTS. (MAŁOPOLSKA MASSIF)
NORTHERN HCMTS. (ŁYSOGÓRY BLOCK)
Fig. 4. Tec tonic sub si dence curves of ana lysed suc ces sions
LO. — Llandeilo, A. — Ashgill, LY. — Llandovery, WEN. — Wen lock, P. — Přidoli; strati graphic scale af ter Harland et al. (1990); bro ken lines in sub - si dence curves rep re sent in ter vals with poor strati graphic con trol
dif fer ences can be at trib uted to con trast ing struc tural set tings: a sta ble cratonic ba sin in the south and a foredeep settting in the north. This im plies that both ar eas are frag ments of larger re - gional units which had been jux ta posed due to some later tec - tonic pro cesses. There fore, the pres ent dis cus sion will fo cus on a wider re gional con text of the study area in or der to ex plain its pres ent struc tural con fig u ra tion.
There are merely scarce data on the Lower Palaeozoic north of the HCMts. doc u ment ing only its up per most part in a few bore holes in the Radom area (Miłaczewski et al., 1983). These ob ser va tions ev i dence that the de vel op ment and thick ness of the up per most Si lu rian to low er most De vo nian are very sim i lar to those of the north ern HCMts. It is re mark able that highly
com pa ra ble de pos its were en coun tered also in the Lublin Trough area. For ex am ple, the low er most De vo nian Sycyna For ma tion de vel oped as ma rine shales sev eral hun dreds metres thick ex tends both in the Łysogóry Block area (near Radom) as well as in the Lublin area (Miłaczewski, 1981).
The well data from the MM area south of the HCMts.
(Jurkiewicz, 1975; Moryc, 1985) are too scarce to en able re li able backstripping cal cu la tions. How ever, they do dem on strate sim i - lar fa cies and sed i ment thicknesseses, sug gest ing pat terns of tec - tonic sub si dence com pa ra ble to the south ern HCMts. In par tic u - lar, the Or do vi cian de vel op ment dis plays re mark able sim i lar ity in the MM area be tween the HCMts. and the Carpathians (Tomczyk, 2000; Tomczykowa and Tomczyk, 2000). It is
SANDOMIERZ KIELCE
4-5
3 4
4
1
1.5 2 3.5
1
1 1
3
the rma l ma turity (CAI units ):
3 Ca mbria n 1 Ordovicia n 1.5 S iluria n
10 km
Wiś niówka Wlk.
Cha bowe Doły Wilków Grucha wka
Za rę by 2
Ws za chów 2 P rą gowie c
P obros zyn
Ubline k 1-bis
Ka mie ń P le b. 1 Os s olin IG 1
Mójcza
Fig. 6. Ther mal ma tu rity of the Lower Palaeozoic de pos its in the Holy Cross Moun tains; see the text for sources of ma tu rity data Ex pla na tions as in Fig. 2
Fig. 5. Modelling of the tec tonic sub si dence of the Bardo Syncline sec tion (vari ant A) as sum ing palaeobathymetric cor rec tions Ex pla na tions as in Fig. 4
400 440 420
480 460 520 500
TECTONIC SUBSIDENCE (m)
Ma
OR DOVICIAN S ILURIAN
TREMADOC ARENIG LLAN-
VIRNLO. CARADOC A. LY. WEN. LUDLOW P.
GREY- WACKES
30 m 50 m
150 m
ze ro pa la e oba thyme try
te ctonic su bside nce a ss uming pa la e oba thyme try 0
100
200
300
S HALLOW-WATER S ILICICLAS TICS
CONDENSED
CARBONATES GRAP TOLITIC S HALES
50 m a s s ume d wa te r de pth
worth stress ing that Up per Si lu rian coarse-grained clastics of con sid er able thick ness (typ i cal of the north ern HCMts.) have not been en coun tered over most of the MM area ex cept for its south - west ern mar gin. The low and rel a tively con stant sub si dence rates seem there fore typ i cal for the Małopolska Mas sif, dis tin guish ing this area from the Łysogóry Block.
Com plete Lower Palaeozoic sec tions are doc u mented in the Podlasie De pres sion and in the base ment of the Lublin Trough, both units clearly within the EEC (Baltica) area (Fig. 1). There, the sed i men tary de vel op ment is sim i lar to that of the ŁB as stressed by Dadlez et al. (1994). More over, backstripping cal - cu la tions by Poprawa and Pacześna (2002) dem on strate that the tec tonic sub si dence pat tern is also sim i lar, dis play ing char - ac ter is tic ac cel er a tion dur ing Lud low and Přidoli. This ev i - dence was used by the pres ent au thor (Narkiewicz, 2000) to in - ter pret the pres ence of a con tin u ous Late Si lu rian foredeep ba - sin ex tend ing from the ŁB area to the east and north in clud ing the EEC (Baltica) mar gin to wards the Peri-Tornquist Ba sin in north ern Po land (Poprawa et al., 1999).
Poprawa and Pacześna (2002) re port that the to tal mag ni tude of the Late Si lu rian tec tonic sub si dence gen er ally in creases to - wards the south west ern EEC mar gin at tain ing val ues of more than 1100 metres in the War saw area (Okuniew IG 1 well). Such mag - ni tude ex ceeds by al most 500 metres the max i mum value ob tained by the pres ent au thor for the Łysogóry (A) vari ant (Fig. 4). Ac - cord ing to Poprawa and Pacześna (2002) the ap par ent lack of a trend of in creas ing sub si dence be tween the Lublin-Podlasie area and the Łysogóry Block seems to con tra dict the in ter pre ta tion of a con tin u ous Late Si lu rian foredeep ba sin ex tend ing east and north of the pres ent MM/ŁB bound ary (Narkiewicz, 2000).
How ever, the ob served ir reg u lar pat tern of Late Si lu rian tec tonic sub si dence in the area dis cussed may be rec on ciled with the con cept of a con tin u ous foredeep ba sin for the fol low - ing rea sons:
1. The SW-margin of the Lublin Trough is a fault zone with a com plex his tory of syn-Variscan (Late Car bon if er ous) and prob a bly also later (syn-Alpine) strike-slip move ments with dextral sense. Al though the to tal dis place ment may have been on the or der of sev eral tens rather than hun dreds of kilometres, it may have af fected to a cer tain de gree the pri mary pat tern of the Lower Palaeozoic ba sin. The re sults of Poprawa and Pacześna (2002) show the de crease in sub si dence from NW to SE and in this di rec tion the data seem to be more con sis tent with the ŁB data (com pare e.g. the Łopiennik IG 1 well in the cited pa per).
2. A pro gres sive trend of grad u ally in creas ing sub si dence to wards the orogen edge would be ex pected only in a case of ho mo ge neous lithospheric plate un der ly ing the foredeep ba sin.
As suming that the ŁB is a dis tinct crustal unit bounded by deeply-rooted dis con ti nu ities, it seems not sur pris ing that it re - sponded in di vid u ally to an orogenic load.
The data on the ther mal ma tu rity of the Lower Palaeozoic north-east of the HCMts. were re ported from the EEC as far as 100 km from the stud ied area (Nehring-Lefeld et al., 1997).
They in di cate lev els of ma tu rity in creas ing to wards the south-west and reach ing up to CAI 4–5, i.e. val ues com pa ra ble to those ob served in the north ern HCMts. Data from the area south of the HCMts. are scarce and lo cated mostly in the west ern part of MM (Belka and Siewniak-Madej, 1996). These re sults re veal a lack of any dis tinct ther mal events in the Or do vi cian to
De vo nian. It may be there fore as sumed that the ex ist ing data, al - though lim ited, point to a con sis tent pat tern of ther mal ma tu rity within both ana lysed re gional units, and a clear con trast be tween them.
In sum mary, the pre sented re sults sug gest that the Or do vi - cian to ear li est De vo nian depositional and sub si dence evo lu tion of the Łysogóry Block gen er ally fol lowed the sce nario known from the un dis pu ta ble EEC — the Podlasie De pres sion and Lublin Trough. It is here in ter preted that the above-named re - gional units were all parts of the same foredeep basinal sys tem ex tend ing from south east ern Po land to wards the north-west, i.e.
along the Baltica mar gin. The pres ent re sults are thus not com - pat i ble with the con cept of the late Early Palaeozoic ac cre tion of the ŁB as a sep a rate terrane (Pożaryski, 1990, see also Pożaryski et al., 1992; Franke, 1995; Unrug et al., 1999).
On the other hand, the Małopolska Mas sif dis played a dif - fer ent sub si dence pat tern and a con trast ing ther mal his tory in the Early Palaeozoic. The MM can be in ter preted as a part of the Or do vi cian to Si lu rian sta ble cold cratonic area be ing ap - par ently “not in place” within the pres ent re gional con fig u ra - tion of the Lower Palaeozoic. It can be safely as sumed that this unit was placed in its ap prox i mately pres ent po si tion rel a tive to the ŁB be fore the on set of the uni form Emsian mar ginal ma rine to con ti nen tal clastic de po si tion which de vel oped in both re - gions of the Holy Cross Mts. (e.g. Szulczewski, 1995; see also data on de tri tal mus co vite ages in the Emsian in Belka et al., 2000). The hy po thet i cal dis place ment of the MM may ex plain the ap par ent lack of an orogenic wedge south and west of the pre sumed foredeep in the ŁB area. In or der to de ter mine the di - rec tion of this trans la tion and the prov e nance of the MM crust it is nec es sary to dis cuss the gen eral biogeographic af fin i ties of the Lower Palaeozoic in the MM area, as well as its palaeomagnetic and sed i ment-provenance con straints.
Most of the biogeographic data from the stud ied area re fer to the Or do vi cian, mainly in the south ern HCMts. (MM). The in ter - pre ta tions based on brachi o pods (re cently e.g. Cocks, 2000), cono donts, ostracods and trilobites (cf. re view by Dzik, 1999) unan i mously point to gen er ally Bal tic af fin i ties. This is in agree - ment with the data on acritarchs (Servais and Fatka, 1997) al - though these are not re ferred to any spe cific ex po sures and thus their af fil i a tion to MM ver sus ŁB is not clear. The data char ac ter - is ing di rectly the north ern Holy Cross Mts. (ŁB) are few. Cono - donts from a sin gle ex po sure in Pobroszyn in clude not only Bal - tic but also Bo he mian and North Amer i can forms (Dzik, 1999).
Palaeomagnetic data, ob tained ex clu sively from the south ern Holy Cross Mts., pro vided a ba sis for con tra dic tory in ter pre ta - tions of the move ment of the Małopolska Mas sif rel a tive to Baltica (EEC). Lewandowski (1993) as sumed right-lateral trans - la tion of the MM along the Baltica mar gin af ter the Early De vo - nian and be fore the Mid dle Car bon if er ous. On the other hand, Nawrocki (2000) ar gued that MM did not un dergo any con sid - er able post-Caledonian right-lateral trans la tion. He claimed that his re cent Bardo diabase study in di cated the ac cre tion of the MM al ready be fore the lat est Si lu rian. A care ful anal y sis of his strati - graphi cal data (par tic u larly those on the un cer tain age of in tru - sion and tec tonic de for ma tions — com pare also Migaszewski, 2002) sug gests how ever that the time of ac cre tion could equally ex tend into the ear li est De vo nian (Lochkovian).
The stud ies of de tri tal ma te rial prov e nance were based on zir cons (Valverde-Vaquero et al., 2000) and mus co vite (Belka et al., 2000) from the Cam brian and Lower De vo nian. The mus co vite data from the MM area point to Cadomian de tri tal ages in the Lower Cam brian and thus, ac cord ing to the cited au thors, prove the Gond wana af fin ity of the mas sif. How ever, this may ap pear a pre - ma ture con clu sion in the light of ob ser va tions by Valverde-Vaquero et al. (2000) who found zir cons of that age — at trib uted to Vendian volcanics — in the EEC (Baltica) area near War saw. Belka et al. (2000) ar gued that their data on mus co vite ages and the com pi la tion of palaeobiogeographic data col lec tively in di cate that the MM has been a part of Baltica since the Mid dle Cam brian (“first Gond wana-derived microplate that accreted to the mar gin of Baltica”). Ac cord ing to these au thors, the Łysogóry
Block prob a bly had been also sit u ated very close (or even at tached) to the Fennoscandian seg ment of Baltica since Late Cam brian time.
How ever, the au thors do not at tempt to in ter pret the mu tual spa - tial-temporal re la tion ships of the MM, ŁB and EEC dur ing ac cre - tion.
The data dis cussed, in par tic u lar those on the biogeography of the Lower Palaeozoic in the MM area, strongly sug gest that the MM was a part of Baltica dur ing the Or do vi cian to Si lu rian in ter val. Hav ing in mind the gen eral palaeogeographic- structural con fig u ra tion in the TESZ area dur ing the Late Si lu - rian, i.e. in the time when pos si ble MM trans la tion oc curred, it seems most prob a ble that the MM was dis placed due to right-lat eral strike-slip move ment along the pres ent SW mar gin of Baltica (=EEC). The op po site sense of trans la tion seems im -
Fig. 7. Hy po thet i cal Late Si lu rian to Early De vo nian de vel op ment of the TESZ in Cen tral Eu rope, con sis tent with the data ana lysed in the pres ent pa per
NGPC — North Ger man-Pol ish Caledonides; other ex pla na tions as in Fig. 1
prob a ble as there was East ern Avalonia crust accreted to the (pres ent) NW of the study area, i.e. in the area of the North Ger - man-Pol ish Caledonides (Pha raoh, 1999; Dadlez, 2000;
Fig. 1). Also in the light of the pres ent knowl edge of con tem po - rary plate ki ne mat ics (Torsvik et al., 1996) the most prob a ble di rec tion of trans la tion would be right-lat eral con sis tent with the sinistral ro ta tion of Baltica (Dadlez, 2000).
Fig ure 7 shows a pos si ble sce nario in clud ing, first, a de vel - op ment of the orogenic wedge and the re lated foredeep ba sin in the HCMts. area, and there af ter, right-lat eral strike-slip move - ment of a part of Baltica com pos ing the pres ent MM. Such a model is also con sid ered prob a ble by Pha raoh (1999) who stressed that the sup posed “Cadomian” (Gondwanan) prov e - nance of the Małopolska terrane is not yet proven and that it may have “...dis persed dextrally along the Tornquist mar gin from a Neoproterozoic source re gion else where in Baltica, rather than cross ing the Iapetus-Tornquist Ocean di rectly...”.
The MM crust could have been orig i nally lo cated close to the pres ent re gion of Dobrogea, as pro posed by Dadlez et al.
(1994) based on re gional com par i sons (Fig. 7). It seems how - ever not un likely that it was lo cated in a more north-west erly po si tion, i.e. closer to the pres ent HCMts.
GENERAL CONCLUSIONS AND IMPLICATIONS
1. The depositional, sub si dence and ther mal de vel op ment of the Łysogóry Block is con sis tent with the pat tern ob served in the ad join ing EEC ar eas. This con tra dicts Pożaryski’s (1990) hy poth e sis on the terrane na ture of this block within the Cal - edo nian orogen (see also Pożaryski et al., 1992; Franke, 1995;
Unrug et al., 1999). The ŁB area is here in ter preted as the part
of a Late Si lu rian foredeep ba sin which de vel oped on the Baltica mar gin in re sponse to last phases of col li sion with the East ern Avalonia (Fig. 7).
2. The de vel op ment of the con tin u ous Late Si lu rian fore - deep ba sin along the Baltica mar gin from the Peri-Tornquist Ba sin in the north-west to the pres ent north ern HCMts. im plies that the North Ger man-Pol ish Caledonides orogen had its NE con tin u a tion near the pres ent Holy Cross Mts. area (Fig. 7).
3. The south ern HCMts. as well as the en tire MM area re - veals an Or do vi cian-Silurian sub si dence de vel op ment, ther mal his tory and crustal struc ture point ing to a sta ble cratonic set - ting. Ex isting sim i lar i ties in sed i men tary suc ces sion (mostly Or do vi cian and Lower Si lu rian) as well as a clearly Bal tic palaeobiogeography in di cate a close spa tial con nec tion be - tween MM and Baltica dur ing the time in ter val ana lysed.
4. The jux ta po si tion of the MM against the ŁB area can be ex plained as sum ing, af ter Dadlez et al. (1994), that the MM is a part of Baltica de tached from its mar gin due to right-lateral strike-slip. The time of such a trans la tion is brack eted be - tween the late Lud low, an in ter val of dis tinctly dif fer ent sub - si dence and sed i men ta tion pat terns in the MM ver sus ŁB ar - eas, and the Emsian.
Ac knowl edge ments. Pre lim i nary sub si dence anal y sis was ac com plished within the frame work of the pro ject led by Dr Zbigniew Kowalczewski to whom I am in debted for valu able in for ma tion and sug ges tions. I also thank Bart Birdsall (Apache Po land), Jan Malec, Wiesław Trela (both PGI Kielce), and Katarzyna Narkiewicz (PGI Warszawa) for pro vid ing un - pub lished ther mal ma tu rity data. Elrzbieta Tarka helped with draw ing the fig ures. Paweł Poprawa is ac knowl edged for re - marks on an ear lier ver sion of the manu script.
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