Piotr Jaglarz

FACIES AND SEDIMENTARY ENVIRONMENT

OF THE CARBONATE-DOMINATED CARPATHIAN KEUPER

FROM THE TATRICUM DOMAIN: RESULTS FROM THE DOLINA

SMYTNIA VALLEY (TATRA MTS, SOUTHERN POLAND)

In sti tute of Geo logi cal Sci ences, Jagiel lo nian Uni ver sity, Ole an dry 2A, 30- 063 Kraków, Po land; e- mail: pi otr.jaglarz@uj.edu.pl

Jaglarz, P., 2010. Fa cies and sedi men tary en vi ron ment of the carbonate- dominated Car pa thian Keu per from the Ta tricum do main: re sults from the Dolina Smyt nia val ley (Ta tra Mts, South ern Po land). An nales So cie ta tis Ge olo go rum Po lo niae, 80: 147–161.

Ab stract: The pa per fo cuses on an in ter pre ta tion of sedi men tary and early dia ge netic en vi ron ment in the carbonate- dominated up per most Lad in ian–No rian suc ces sion from the Ta tricum do main of the Ta tra Moun tains as well as its con trol ling fac tors. Lime stones with cherts are the prod uct of pedo genic pro cesses, formed dur ing long- term ex po sures of car bon ate sub strate. Chal ced ony cherts were formed dur ing rela tively early dia gene sis of pedo genic lime stones. Dolostones and dolo mitic mud stones were de pos ited in a kind of salt marshes. Pseu do -morphs af ter sul fates and ab sence of ben thic fauna in di cate in creased sa lin ity and in ten sive evapo ra tion. Ad di tion ally, low TOC con cen tra tion sug gests a low pro duc tiv ity in the ba sin. On the con trary, sta ble iso tope sig nals in di cate that the sedi men tary en vi ron ment was strongly af fected by me te oric wa ter. Moreo ver, d18O and con cen tra tion of Sr sug gest that dolostones were formed un der the in flu ence of both ma rine and me te oric wa ters. Dolo mitic mud stones could be de pos ited in a salt- marsh en vi ron ment fed by dis tal sheet floods. Com po nents of paly no logi cal ma te rial and or ganic com pounds in black dolo mitic mud stones in di cate the ter res trial ori gin of or ganic mat ter. Dolo mitic re go liths were formed as the re sult of sub aer ial ex po sure and kar sti fi ca tion of dolo-stones. Coarse- grained sili ci clas tics and varie gated mud stone are in ter preted, re spec tively, as a flu vial chan nel and flood plain fa cies of ephe meric flu vial en vi ron ment. Sedi men tary en vi ron ment of the Keu per sedi ments was con trolled by two main fac tors: synsedi men tary tec tonic move ments and cli mate changes. In the lat est Lad in ian, the Mid dle Tri as sic car bon ate plat form was emerged, what re sulted in the de vel op ment of pa laeo sols. Block tec tonic move ments af fected the Ta tricum Ba sin in Keu per time. Horsts were emerged, whereas troughs were filled with flu vial or salt marsh sedi ments. In ten sive tec tonic move ments are sug gested by seismic- generated slumps and abrupt fa cies changes. More in ten sive chemi cal weath er ing and in ten sive con tri bu tion of pure sili ci clas tics sug gest cli mate plu vi ali za tion in late Lad in ian–early Car nian time. On the con trary, domi na tion of physi cal weath er ing in di cates the aridi za tion of cli mate in late Car nian?–No rian time. The up per Car nian?–No rian suc ces sion was formed in hot and semi- arid cli mate con di tions. Long- term cli mate changes was masked by short- term cli mate fluc tua tions. Geo chemi cal in di ca tors sug gest that dolostones rep re sent more hu mid pe ri ods, whereas dolo mitic mud stones rela tively dry pe ri ods.

Key words: tec ton ics, cli mate, dolostones, pa laeo sols, up per most Lad in ian–No rian, High- Tatric Unit, West ern Car pa thi ans.

Manu script re ceived 5 May 2009, ac cepted 15 July 2010

IN TRO DUC TION

By the end of the Ladinian, fun da men tal fa cies changes oc cured in the Ta tricum Ba sin. The Mid dle Tri as sic car bon -ate plat form was emerged, and un der went ero sion and pedogenic pro cesses. In the Car nian–No rian pe riod, sedi -ments of the so called Car pa thian Keu per were de pos ited. The sedi ments of this pe riod de vel oped in two li tho fa cies: con ti nen tal clas tics (red beds type) and shal low ma rine car -bon ates. For in stance, the seqence of Dolina Smyt nia val ley

rep re sents the suc ces sion with car bon ate sedi ment domi -nance.

Sedi men tary and diagenetic en vi ron ment of the Car pa -thian Keu per were sub ject to re search by sev eral authors, but they have mostly been fo cused on the Fa tricum Ba sin (Al- Juboury & Du ro viè, 1992, 1996; Rych li ñski, 2008). So far, there were no sedi men to logi cal analy ses con ducted for analo gous de pos its from the Ta tricum do main, al though

some min era logi cal and petrographic as well as stratigra-phical in ves ti ga tions have been car ried out (Turnau-Morawska, 1953; Ko tañski, 1956b). Scarce oc cur rence of the dis cussed sed i ments was caused by the ero sion af ter Old Cimmerian tec tonic move ments at the Tri as sic/Ju ras sic bound ary (Ko tañski, 1956a, 1959a, 1961) and gen eral high sus cep ti bil ity of rocks to the weath er ing.

The main goal of this pub li ca tion is an in ter pre ta tion of sedi men tary en vi ron ment, and its con trol ling fac tors in the carbonate dominated up per most Lad in ian–No rian suc ces -sion from the Ta tricum do main in the Ta tra Mts. In ad di tion,

fur ther as sess ment of con di tions dur ing dolo miti za tion and si lici fi ca tion of car bon ates is pre sented.

GEN ERAL SET TING

The Ta tra Mts are the high est and farthest north- located mas sif of the Cen tral West ern Car pa thi ans. It com prises the Varis can crys tal line core and strongly de formed Lower Tri as sic–mid Cre ta ceous rocks. Crys tal line base ment is cov -ered by sub se quent auto chthonous (lo cally

parautochtho-Fig. 1. Lo ca tion of the stud ied sec tion (af ter: Bac-Moszaszwili et al., 1979; mod i fied). A. Lo ca tion of the Dol ina Smytnia val ley re gion in the tec tonic-sketch map of the Tatra Mts B. Lo ca tion of the stud ied sec tion in the geo log i cal map of the Dol ina Smytnia val ley re gion

nous; Du mont et al., 1996) rocks and lo cal over thrust of Czer wone Wier chy (lower) and Gie wont (up per) nap pes (Ko tañski, 1961, 1979b; Pas sen dor fer, 1961). The above men tioned tec tonic ele ments form the High- Tatric Unit which is cov ered by the lower (Krížna) and up per (Choè) Sub- Tatric nap pes (Fig. 1A).

Sedi ments of the High- Tatric Unit were de pos ited in the Ta tricum Ba sin (An dru sov et al., 1973; Ko tañski, 1979b) that dur ing the Tri as sic was confined to the north ern part of the Car pa thian seg ment of the West ern Te thys and situ ated on the south ern edge of the North- European Plat form (Kozur, 1991; Mi chalík, 1993, 1994).

Oc cur rence of the Up per Tri as sic sedi ments of the High-Tatric Unit is lim ited to the auto chtho nus cover. The Carpathian Keu per suc ces sion is de vel oped in two fa cies: sili ci clas tic and car bon ate. Some se quences are de vel oped in clastic fa cies, whereas in other sec tions the Car pa thian Keu per is de vel oped as a com plex of dolostones (Turnau-Morawska, 1953; Ko tañski, 1956b, 1959a, c, 1979a; Wój-cik, 1959), oc ca sion ally, as in the Dolina Smyt nia val ley, with sev eral metre- thick in ter ca la tions of sili ci clas tics within dolostones (Fig. 2).

Keu per sedi ments are de void of any in dex fos sils. There fore, it is dif fi cult to es tab lish their age pre cisely. Car -bon ate sedi ments from the Dolina Smyt nia val ley sec tion are con sid ered as equiva lent to the Car pa thian Keu per sili ci clas tics (Ko tañski, 1956b). Ko tañski (1956b) as signed car -bon ate-clastics and dolostones to the Car nian and No rian, re spec tively (Fig. 2).

Depo si tion of the Keu per sedi ments was pre ceded by emer gence of the Mid dle Tri as sic re stricted car bon ate ramp, de vel oped in dry and hot cli mate con di tions (Jaglarz & Szulc, 2003). Emer gence of the car bon ate ramp was ac com pa nied by ero sion and pa laeo sol for ma tion (Jaglarz & Rych li ñski, 2005; Jaglarz, 2007). Jaglarz (2007) proved that pa -laeo sols (see be low) from the base of the Dolina Smyt nia val ley se quence may be of the lat est Lad in ian or the ear li est Car nian age (Fig. 2).

Sedi ments of vari ous ages over lie the Keu per de pos its. In the Czer wone ¯lebki area, red bed sili ci clas tics are re placed by con ti nen tal sedi ments of the To ma nová For ma -tion (up per No rian–Rhae tian) con sist ing of plant- bearing dark mud stones and quartz itic sand stones (Ra ci bor ski, 1891; Ko tañski, 1959a, c; Mi chalík et al., 1976, 1988; Fija³kowska & Uch man, 1993). In the Dolina Chocho³ow-ska area, the Rhae tian ner itic sedi ments, com posed of black mud stones and or gan ode tritic lime stones with Rhaetina

gre garia, rests on sili ci clas tics (southern slope of Bo brow

-iec Mt) or dolostones and clas tics (Prze³êcz w Ku lawcu pass) of the Keu per (Ko tañski, 1959c, 1979a; Rad wañski, 1968). Lower Ju ras sic ma rine sedi ments rest on the ero -sively trun cated No rian dolostones in the Dolina Smyt nia area (Ko tañski, 1956b; Rad wañski, 1959).

MA TE RI ALS AND METH ODS

In ves ti ga tions en com pass the up per most Ladinian– Norian suc ces sion of the High-Tatric Unit from the Dol ina Smytnia val ley in the West ern Tatra Mts (Fig. 1). De tailed

sedimentological field stud ies were sup ple mented by microfacies ob ser va tions. The re spec tive val ues of d13C and d18O were de ter mined us ing mea sure ments made with mass spec trom e ter SUMY, at the In sti tute of Geo log i cal Sci ences, Acad emy of Sci ences of Belarus at Minsk. The sam ples were treated with 100% orthophosphoric acid. Car -bon di ox ide was then col lected in a trap with liq uid ni tro gen and pu ri fied in vac uum. Mea sure ment er ror was ±0.2‰. Sta ble iso tope ra tios in car bon ate sam ples are pre sented in this pa per in ref er ence to the PDB stan dard.

Main ele ments were ana lyzed with In duc tively Cou pled Plasma- Atomic Emis sion Spec trome try (ICP- ES) method. For this pur pose, se lected rock sam ples (0.2 g in weight) were mixed with LiBO2 and heated. The mix ture was then

cooled down and dis solved in HNO3 (5%). Com po si tion of

the so lu tion was ana lyzed with ICP ES spec trome ter. In -duc tively Cou pled Plasma- Mass Spec trome try (ICP- MS) was used for stron tium analy ses. Prepa ra tion of sam ples were analo gous to the ICP ES method. Sub se quently, com -po si tions of so lu tions were ana lyzed by mass spec trome ter. Analy ses of main and trace ele ments were car ried out at the Acme Ana lyti cal Labo ra to ries Ltd. (Van cou ver, Can ada).

For to tal or ganic car bon (TOC) con tent, 10 g rock sam -ples were ana lysed with the Leco method. Or ganic car bon con tent is the dif fer ence be tween to tal car bon and graph ite con tents. To tal car bon con tent was mea sured with the Leco method and graph ite con tent was es tab lished by roast ing the sam ples at a tem per a ture of 600 °C and wash ing them out with hy dro chlo ric acid (HCl). Anal y ses were car ried out at the Acme An a lyt i cal Lab o ra to ries Ltd. (Van cou ver, Can ada). One sam ple of black mudstone was ana lysed by the Rock Eval method at the Pe tro leum Geo chem is try Lab o ra tory, Uni ver sity of Sci ence and Tech nol ogy (Kraków, Po land).

A sam ple of about 100 g was sub ject to or ganic geo chem i cal anal y ses. It un der went 24 h ex trac tion us ing Soxh -let’s ap pa ra tus with di chloro methane (DCM) and meth a nol (7.5:1, v/v). The sol vents were then evap o rated from the ex -tracts to dry ness with a ro tary, vac uum evap o ra tor. Or ganic com pounds were ini tially fractioned ac cord ing to a pro ce -dure de scribed by Rospondek et al. (1994). The res i dues were dis solved in a small vol ume of di chloro methane (DCM). The DCM was then evap o rated and the ex tract was weig hed, and then frac tion ated by ad sorp tive chro ma tog -ra phy col umn (Bochwic, 1975). The col umn (80×5 mm) was packed with Al2O3 (ac ti vated for 2 h at 130 °C) and

washed with n-hex ane be fore use. The mix ture was introduced to the col umn, af ter dry ing on a small quan tity of Al2O3. The ex tract was sep a rated into two frac tions: aliphatic

(satura ted) hy dro car bons eluting with nhex ane, and ar o -matic hy dro car bons eluting with n-hex ane/DCM (9:1, v/v). Af ter sol vents re moval, the frac tions were weighed.

Com po si tion of ali phatic and aro matic hy dro car bon frac tions was ana lysed by the Gas Chromatography- Mas Spec tros copy (GC- MS) method. The GC- MS analy sis was car ried out on an Ag ilent 6890 gas chro ma tograph cou pled to an Ag ilent 5973 Net work with mass se lec tive de tec tor (MSD) in the De part ment of Geo chem is try, Min er al ogy and Petrog ra phy, Uni ver sity of Sile sia (Sos now iec, Po land) ac -cord ing to a pro ce dure pre sented by Ro spon dek et al. (2009).

Fig. 2. Up per most Ladinian–Norian se quence from the Dol ina Smytnia val ley. Tec tonically-con trolled shallowing-up ward cy cles (dark tri an gles) and se lected chem i cal in di ca tors. Chronostratigraphy af ter Kotañski (1956b), mod i fied by Jaglarz (2007). L3 – 3rd or der depositional se quence at the top of Ladinian suc ces sion

DOL INA SMYTNIA VAL LEY SEC TION

The Dol ina Smytnia val ley sec tion was men tioned by Zejszner (1852) and Uhlig (1897) who con sid ered it as “lower Tri as sic”. Later it was in ves ti gated by Turnau-Morawska (1953) and Kotañski (1956b, 1959b).

The discussed sec tion is lo cated in the east ern part of the Kominiarski Wierch mas sif, at 1250–1300 m above sea level (Fig. 1B). The section is re versed and in clined to the south-west (an gle of in cli na tion is about 65°). The investi-gated se quence is about 50 m thick (Fig. 2).

Lime stones with cherts (4 m thick), form ing the top of the Ladinian se quence, oc cur in the lower part of the suc ces -sion, and de pos its dom i nated by al ter nated dolostones and dolomitic mudstones, in the up per part of the se quence. Con glom er ate, sand stones and var ie gated mudstones of few me ter-thick oc cur in the mid dle part of dolostone-mud-stones com plex. The top of the Up per Tri as sic se quence is eroded and cov ered by Lower Ju ras sic sed i ments (Radwañ-ski, 1959; £uczyñ(Radwañ-ski, 2001).

RE SULTS

The lithofacies de scribed be low can be grouped into sev eral fa cies as so ci a tions. Dolostones, green and black dolomitic mudstones and dolomitic regoliths are con sid ered as a salt marsh fa cies. Lime stones with cherts are clas si fied as pedogenic fa cies, linked with long-term ex po sure of the Mid dle Tri as sic car bon ate plat form. Pure siliciclastic de -pos its in turn, rep re sent con ti nen tal red bed type sed i ments.

Dolostones

Dark to lightgrey dolostones are gen er ally well bed -ded. Bed thick nesses are from 8 to 70 cm. Only dolostones from the lower part of the seqence are faintly bed ded. The dolostones are of ten lam i nated; dark laminae are al ter nated with light laminae con tain ing dis persed do lo mite crys tals. Laminae are of ten plas tic ally de formed (Fig. 3A, B). Micri-tes and microspariMicri-tes dom i nate among dolo- stones (Fig. 3D). Fenestral struc tures are dis tinc tive for dolostones from the up per part of the suc ces sion (Fig. 3C).

Grain-sup ported dolomitic con glom er ate (few dozen of centi metres thick) with well-rounded clasts (2 to 10 mm in di am e ter) and ero sive ba sic sur face oc cur in the dolostone suc ces sion (Fig. 4C). Ho ri zons of brec cias were also found (Fig. 5).

Dolostones are al ter nated with green or black mudsto-nes (Fig. 4A). The thickmudsto-ness of dolostone beds is greater than mudstone beds, and bound aries be tween them are usu -ally sharp.

In ter pre ta tion

Lam i nated dolostones are in ter preted as stromatolites. Dis persed do lo mite crys tals are con sid ered as fine pseudo morphs af ter sul fates (Fig. 3A–B). Some laminae de for ma -tions in the de scribed rocks are con sid ered as enterolithiclike struc tures (Fig. 3A). For ma tion of such struc tures re -sulted from re cur rent hydratation and dehydratation of Ca-sul fates in the pro cess of al ter nate cap il lary rise and fall of

brines (cf. Álvaro et al., 2000; Schreiber & El Tabakh, 2000).

Dolostones with fenestral struc tures are rec og nized as thrombolites. Fenestral struc tures are a re sult of dry ing or de cay ing microbialites (Shinn, 1968). De cay of microbiali-tes is more prob a ble be cause of cha otic ar range ment and irregular shape of fenestra, al though their shape mod i fi ca -tion by evaporites cannot be excluded.

Dolomitic con glom er ates with ero sive bot tom sur face, iden ti fied in the up per part of the se quence (Fig. 4C), are a re sult of redeposition of eroded sed i ments dur ing highen -ergy event. Most of intraclasts were prob a bly de rived from des ic cated sed i ments dur ing an ep i sode of emersion (cf. Platt, 1989; Muir et al., 1980).

Dolostones were pre sum ably de pos ited in a periodically emerged shal lowma rine en vi ron ment. It was prob a -bly a kind of backshore marsh. Pseudo morphs af ter sul fates, ab sence of fauna and bioturbational struc tures in di cate an in ten sive evap o ra tion and increased salinity.

Green and black dolomitic mudstones

Lam i nated dolomitic mudstones are green and black (Fig. 4B). They are com posed of siliciclastics dom i nated by quartz and dolomitic ma trix. Green dolomitic mudstones are up to 3 cm thick, and black dolomitic mudstones are up to 20 cm thick. Black dolomitic mudstones oc cur in the up per part of the se quence (Fig. 2). Opaque phytoclasts and sporo- morphs were dis tin guished among palynological com po -nents of black dolomitic mudstones (Annette Götz, pers. commun., 2006).

In ter pre ta tion

Green and black dolomitic mudstones al ter nat ing dolo-stone beds (Fig. 4A) are con nected with pe ri odic in put of ter res trial clastics. Green col our of mudstones dom i nat ing in the lower part of the se quence sug gests reductive con di -tions in the sed i men tary en vi ron ment (McBride, 1974). This, in turn, is an in di ca tor of fre quent flood ing or high level of ground wa ter (Turner, 1980; Aigner & Bachmann, 1989). Black col our of mudstones from the up per part of the se quence in di cates the pres ence of non-de com posed or ganic mat ter de pos ited in sub aque ous en vi ron ment (McBride, 1974). Dolomitic mudstones are prob a bly the ef fect of sed i men ta tion by dis tal sheet floods caused by spo radic, in ten -sive rain falls. How ever, ae olian de po si tion of siliciclastic com po nents of dolomitic mudstones can not be ex cluded (cf. Aigner & Bachmann, 1989; Reinhardt & Ricken, 2000).

Dolomitic regoliths

Dolomitic regoliths (about 2 m thick) rest on the rough sur face of the host dolostones. They con sist of yel low claystones (sev eral to 20 mm thick) al ter nat ing with beds, lenses and rounded clasts of dolostones (Fig. 6).

In ter pre ta tion

Dolostones with flasers of yel low dolomitic claystones are in ter preted as regoliths, and rest on karstified sur face of the host dolostones (Fig. 6). They com prise clay min er als en riched in ox i dized fer ric com pounds, which rep re sent kars- tic re sid uum af ter dis solved car bon ates. Dolomitic

clasts within clayey-car bon ate ma trix dis play rounded edges, what is a proof of their par tial dis so lu tion dur ing ini -tial pedogenic pro cesses (Wright & Wil son, 1987). Dolomitic regoliths were formed as the re sult of subaerial ex po -sure and karstification of dolostones.

Lime stones with cherts

Lime stones with cherts in clude grey and grey-yel low sandy lime stones and sandy dolomitic lime stones. Limesto-nes with cherts are com posed of rounded clasts and nod ules of lime stones, sandy lime stones and dolomitic sandy lime stones and ma trix con sist ing of car bon ate micrites or mi -crosparites. Car bon ate nod ules dis play blurred bound ary

with ma trix (Fig. 7A, B). Mono- and polycrystalline quartz grains (up to about 30%) are dis persed in the ma trix (Fig. 7C, E). Quartz grains are rounded. Chal ce dony cherts and crys tal line forms of fer ric ox ides and hy drox ides com monly oc cur (Fig. 7A, D). Lime stones with cherts are bioturbated (Fig. 7D, E). Bioturbational struc tures (rhi zoids) are of ten filled with sparry cal cite, cherts or with ma trix sed i ment (Fig. 7E).

In ter pre ta tion

Lime stones with cherts are in ter preted as palaeosol. Lime stone and dolomitic clasts rep re sent frag ments of host rocks, which re peat edly un der went weath er ing and

pedoge-Fig. 3. Dolostones. A. Lam i nated dololutite, dark laminae are mi cro bial in or i gin. Sed i ment de for ma tions in the up per part (ar rows) in ter preted as enterolithiclike struc ture. B. De tails of A. Dark laminae mi cro bial in or i gin, light laminae in clud ing do lo mite crys tals in ter -preted as pseudo morphs af ter evaporites (ar rows); thin sec tion. C. Thrombolites with fenestral struc tures, which were caused by de cay of microbialites; thin sec tion. D. Dololutite with sty lo lites; thin sec tion

nesis (Fig. 7B). Round ness of car bon ate clasts is in ter preted as their par tial dis so lu tion in vadose zone (Wright & Wil son, 1987). Sim i larly, lime nod ules are rec og nized as the ef -fect of dis so lu tion and re-pre cip i ta tion of cal cium car bon ate

(Fig. 7A, B). Ma trix-sup ported frame work clasts and grains are the ef fect of pedoturbation (Fig. 7B, E). Bioturbations were caused by the root ac tiv ity. Rhi zoids are the most sig nif i cant fea tures in di cat ing pedogenic or i gin of the dis

-Fig. 4. Dolostone-dolomitic mudstone com plex. A. Dolostones al ter nated with black dolomitic mudstones. B. Lam i nated dolomitic mudstone. Light laminae en riched with quartz grains; thin sec tion. C. Dolomitic con glom er ates. Ero sive sur face marked by white line

Fig. 5. Seis micallygen er ated struc tures. A. Seis micallygen er ated slump brec cia in dolostone and dolomitic mudstone com plex. Ro -tated blocks (R). White rect an gle shown in Fig. 5B. B. Slab of seis mic-gen er ated brec cia marked with white rect an gle in Fig. 5A. Shear sur faces are marked with white lines

cussed de pos its (Fig. 7D, E). Lime stones with cherts were formed by pedogenic pro cesses dur ing long-term ex po sure of car bon ate sub strate.

Con glom er ates, sand stones and var ie gated mudstones

Grain-sup ported quartz con glom er ates (grains sev eral millimetres across) and coarse-grained sand stones are light- grey or pink ish. Grains are well-rounded and their sort ing is poor to me dium. Ma trix is si li ceous or clayey. Fine-grained red sand stones are quartzitic wackes and arenites with si li -ceous-clayey-ferrigenous ma trix. Var ie gated mudstones are quartzitic mudstones and very fine-grained wackes with clayey-si li ceous-ferrigenous ma trix.

Fig. 6. Dolomitic regoliths. Karstified host dolostones (HD). Dolomitic clasts within clayey-car bon ate ma trix dis play rounded edges (ar row)

Fig. 7. Pedogenic lime stones with cherts. A. Nod u lar pedogenic lime stone with red dish cherts (Ch). Cherts are lo cally crushed (ar row). B. Nod u lar pedogenic sandy lime stone. The parts of clasts have faint lim its with ma trix (ar row). Ma trix-sup ported clasts in ter preted as the re sult of root pen e tra tion. C. Cor ro sion traces – polycrystalline quartz grain re placed by car bon ates (ar rows; thin sec tion, x nicols). D. Biodeformed pedogenic lime stone with cherts (Ch). Rhizoid filled with the sur round ing sed i ments (ar rows); thin sec tion. E. Biodeformed pedogenic lime stone. Light grains (quartz) are dis persed in the re sult of the ac tiv ity of roots. Bioturbation struc tures filled with sparite cal -cite ce ments (ar row); thin sec tion

In ter pre ta tion

Pure siliciclastics are in ter preted as the ephemeric flu -vial red bed-type fa cies (see Jaglarz, 2007). Coarse-grained siliciclastics are in ter preted as flu vial chan nel de pos its. Fine-grained red arenites, wackes and var ie gated mudstones can be con sid ered as overbank de pos its. Arenites and wackes prob a bly rep re sent cre vasses whereas var ie gated mudstones flood plains.

GEO CHEM I CAL DATA

Mag ne sium ox ide (MgO) con tent in dolostones ranges from 19.7 to 20.7 wt.%. For regoliths and lime stones with cherts the con tent is 19.3% and 2.8 to 8.4 wt.% of MgO, re -spec tively. The contents of SiO2 in dolostones, dolomitic

mudstones, dolomitic regoliths and lime stones with cherts, are 1.8 to 5.2%, 18.4 to 26.4%, 5.6 and 3.5 to 15.1 wt.%, re -spec tively (Ta ble 1). Av er age con tent of Sr in dolostones is 103±30 ppm and var ies be tween 71 and 143 ppm.

The val ues of d13_{C and d}18

O for dolostones fall in the range of –0.6 to 1.3‰ (av er age 0.4±0.7‰) and –6.0 to –1.9‰ (av er age –3.8±1.4‰), re spec tively. d13C in black and green dolomitic mudstones are –0.1 to 0.6‰ and 1.8‰ re spec tively, d18O were de fined on –4.5 to –4.2‰ and –4.1‰, re spec tively. The d13C and d18O of dolomitic regoliths are –0.6 to 0.2‰ and –4.5 to –3.9‰, re spec tively. Fi -nally, d13C and d18O lime stone with cherts are –6.5 to –5.0‰ (av er age –5.9±0.8‰) and –10.1 do –4.7‰ (av er age –7.3±2.7‰), re spec tively (Ta ble 1).

TOC con tent in dolostones, dolomitic regoliths and lime stones with cherts does not ex ceed 0.04 wt.%, but reaches 2.92 wt.% in black dolomitic mudstones (Ta ble 1).

El e men tary sul phur is the main com po nent of apolar (sat u rated) frac tion of or ganic sub stance in black dolomitic mudstones. Aliphatic hy dro car bons were also iden ti fied with chain length rang ing from C18 to C30, with max i mum

of n-C25. Phytane, pristane and nor-pristane are also pres ent

in sig nif i cant amounts (Fig. 8). Phenantren and methylophe- nantren pre dom i nated in the ar o matic hydrocarbon fraction.

DIS CUS SION

The pres ence of fresh-wa ter dur ing de po si tion of the dis cussed sed i ments is con sid ered as the main rea son of d13

C de creases, be cause freshwa ter is en riched in light car -bon iso topes of or ganic or i gin (Scholle et al., 1992; Peryt & Scholle, 1996; Chafetz & Zhang, 1998).

In flu ence of tem per a ture and evap o ra tion is very low in the case of car bon sta ble iso tope frac tion ation (Moore & Druckman, 1981; Tucker & Wright, 1990, p. 384). There -fore, d13

C is much better in di ca tor of ma rine ver sus me te -oric wa ter con tri bu tion than d18O in the sed i men tary en vi ron ment (Szulc, 2000). En rich ment of de pos its in heavy sta -ble iso tope of ox y gen is the ef fect of evap o ra tion, whereas en rich ment in light iso tope is the re sult of freshwa ter in flu -ence or in crease of flu ids tem per a ture (cf. Hud son, 1977; Peryt & Magaritz, 1990; Lintnerová & Hladíková, 1992).

Pedogenic lime stones show neg a tive val ues of d13C (Ta ble 1; Fig. 2). Neg a tive d13

C val ues are caused by fresh wa ter en riched in iso to pi cally-light, soil-de rived CO2 (cf.

Platt, 1989; Aziz et al., 2003). Prob a bly, the up per part of

Ta ble 1

Con cen tra tion of se lected el e ments and value of geo chem i cal in di ca tors in the Dol ina Smytnia val ley se quence

Samples SiO2 (%) MgO (%) Si (%) Al (%) K (%) Ti (ppm) Sr (ppm) Al2O3/SiO2 K/Al d13 CPDB (‰) d18 OPDB (‰) TOC (%) 1(W) 3.50 8.43 1.64 0.37 0.17 180 426 0.20 0.47 -6.5 -10.1 0.03 2(W) 6.54 2.78 3.06 0.31 0.15 180 641 0.09 0.49 -5.0 -7.1 0.03 3(W) 15.07 4.51 7.05 0.78 0.42 420 357 0.10 0.54 -6.2 -4.7 0.03 4(D) 5.21 19.65 2.44 0.95 0.56 480 71 0.34 0.60 0.7 -3.8 0.03 5(D) - - - -0.6 -3.9 -6(D) 2.87 20.22 1.34 0.51 0.27 240 92 0.33 0.54 -0.1 -4.2 0.04 7(GM) - - - 1.8 -4.1 -8(D) 1.82 20.70 0.85 0.42 0.22 180 106 0.43 0.54 1.3 -2.1 0.03 9(R) 5.57 19.26 2.60 1.03 0.72 420 134 0.35 0.70 0.2 -4.5 0.03 10(R) - - - -0.6 -3.9 -11(D) - - - 0.7 -5.0 -12(BM) 26.38 12.83 12.33 5.22 4.48 2578 76 0.37 0.86 0.6 -4.5 0.33 13(BM) 18.36 13.45 8.64 3.60 3.43 2000 92 0.37 0.95 -0.1 -4.2 2.92 14(D) - - - 0.1 -6.0 -15(D) 1.84 19.92 0.86 0.39 0.28 180 143 0.40 0.72 1.3 -1.9 0.04 16(D) - - - 0.0 -3.7

pedogenic lime stones is en riched in heavy ox y gen iso tope as a re sult of in ten sive evap o ra tion in the top of soil pro file (Liu et al., 1996). Di ver gence of d13_{C and d}18

O curves in the top of dolomitic regoliths can be sim i larly in ter preted (Fig. 2).

Val ues of d13C in dolostones and dolomitic mudstones vary be tween –0.6 to 1.8‰ (Fig. 2). The d13

C value of ma -rine wa ter amounts to over 0‰ (see Hoefs, 1997, p. 156; Tucker & Wright, 1990, p. 384), but in Up per Tri as sic rocks it was be tween 1.5 to 3.5‰ (Korte et al., 2005). Thus, the dis cussed dolostones seem to be en riched in light car bon iso topes. Dolomitization causes in sig nif i cant mod i fi ca tions in orig i nal com po si tion of sta ble car bon iso topes (cf. Tucker & Wright, 1990, p. 384). Based on that, it can be stated that dolostones en rich ment in light sta ble car bon iso -tope re flects the in flu ence of fresh-wa ter dur ing de po si tion of host sed i ments. It seems that orig i nal com po si tion of sta -ble car bon iso tope was pre served. Late diagenetic pro cesses (e.g., recrystalization, cal ci fi ca tion) would prob a bly re sult in more ho mo ge neous iso to pic value in dolostones.

EARLY DIAGENESIS

Dolomitization

Early diagenetic dolomitization is in di cated by the pres -er va tion of orig i nal sed i men tary struc tures (e.g., lam i na tion, bed ding), fine grains, high con cen tra tion of siliciclastics, the pres ence of pseudo morphs af ter sul fates and the ab sence of fauna in dolostones (Sarin, 1962; Veizer, 1970; Peryt & Scholle, 1996). All the above fea tures, slump brec cias, con glom er ates and regoliths con tain ing dolostone clasts sug -gest that the in ves ti gated dolostones are early-diagenetic.

Gen er ally, among early diagenetic dolostones prod ucts of hypersaline or mixed-wa ter can be dis tin guished (Folk & Land, 1975; Hardie, 1987). Hypersaline dolostones con tain higher con cen tra tion of stron tium (Sr) than those formed in mixed zone (Tucker & Wright, 1990, p. 380). In gen eral, con cen tra tion of Sr in the dis cussed dolostones (Ta ble 1) is lower than Sr con tent in early diagenetic dolostones of hy -persa line en vi ron ments (100–600 ppm ac cord ing to Veizer

& Demoviè, 1974). More over, the dis cussed dolostones con tain much less of Sr than dolostones of com pa ra ble age from other parts of the Cen tral Carpathians (145–1010 ppm; Al-Juboury & Duroviè, 1996).

Dolomitization mod i fies the sta ble ox y gen iso tope com po si tion. It de pends on the tem per a ture of pre cip i ta tion and iso to pic com po si tion of dolomitizing so lu tions (Tucker & Wright, 1990, p. 384). En rich ment of sed i ments in heavy ox y gen iso tope re flects in ten sive evap o ra tion whereas en rich ment in light ox y gen iso tope is the re sult of the in flu -ence of me te oric wa ters dur ing dolomitization (Ward & Halley, 1985; Peryt & Magaritz, 1990; Spötl & Burns, 1991). Broad range of d18

O in di cates that dolostones were formed un der the in flu ence of both me te oric and ma rine wa -ters (Ta ble 1; Fig. 2). Sed i men tary fea tures, con cen tra tion of Sr, and d18O in di cate that the dis cussed dolostones were formed dur ing early diagenesis in hypersaline en vi ron ment with pe ri odic in flux of fresh-wa ter. Salt marshes are a very prob a ble en vi ron ment of dolomitization.

Sili ci fi ca tion

Chal ce dony cherts oc cur only within pedogenic lime stones. Cor ro sion of de tri tal quartz grains sug gests that sil ica orig i nated from dis so lu tion of those grains (Fig. 7C), al though clay min er als could also be the source of sil ica. Dis -so lu tion of sil ica oc curs in strongly al ka line en vi ron ment (pH>9; Fried man & Shukla, 1980; Sonnenfeld, 1992). This phe nom ena is com mon in cal crete (e.g., Summer field, 1983). Cur rently, chal ce dony re places car bon ate ma trix (Fig. 7A, D). Sil ica pre cip i ta tion prob a bly oc curred when pH of the en vi ron ment de creased by weath er ing and ox i da -tion of fer rous sul fides (cf. Chafetz & Zhang, 1998). It is con firmed by the oc cur rence of fer ric ox ides and hy drox ides in the dis cussed de pos its. Fer rous sul fides were prob a -bly formed as a re sult of re duc tion of sul fates in con tact with or ganic car bon com pounds (cf. Palmer, 1995). Pres -ence of or ganic car bon in the stud ied pedogenic lime stones is in di rectly con firmed by low d13C value (Ta ble 1; Fig. 2).

SYNSEDIMENTARY TEC TON ICS

Seis mically-gen er ated struc tures

Seis mic shocks in car bon ates, which are dis tin guished by the pro gres sive lithification, are re corded by the tier ing of de for ma tions (Szulc, 1993). The ear lier, lithified sed i -ments un der went brit tle de for ma tions (e.g., synsedimentary faults) whereas the youn ger ones un der went plas tic de for -ma tions or ho mog e ni za tion. Intra-for -ma tion brec cias, interpreted as slump brec cias oc cur within dolostones. In men -tioned brec cias, plas tic ma te rial was alocated along shear while blocks of ear lier lithified sed i ment were ro tated (Fig. 5).

Tec tonically-con trolled cy cles and fa cies-di ver sity

Three shallowing up ward cy cles were dis tin guished in the Dol ina Smytnia val ley se quence (Jaglarz, 2007). The top of pedogenic lime stones form ing the up per most part of the Ladinian depositional L3 se quence makes the bound ary of the first cy cle (Fig. 2). The first cy cle is com posed of al

-Fig. 8. Gas chromatogram of the aliphatic hy dro car bon frac -tion. Or ganic mat ter from black dolomitic mudstones. C18–C30: al -kanes; pristane (Pr), phytane (Ph)

ter nat ing dolostones and green dolomitic mudstones pass ing up ward into faintly bed ded dolostones. Seis micallyin -duced slumps were rec og nized within this com plex (Fig. 5). Var ie gated mudstones form the up per most part of the cy cle. The thickness of the first cy cle is 12 m. Eroded top of the var ie gated mudstones makes the bound ary of the sec ond cycle. Fine- grained con glom er ates, coarse-grained and red fine-grained sand stones be gin the sec ond cy cle. Siliciclas-tics pass up ward to al ter nat ing dolostones and black dolo-mitic mudstones. The top of the dolodolo-mitic com plex is karstified form ing dolomitic regoliths. The sec ond cy cle is 15 m thick. The top of dolomitic regoliths makes the bound -ary of the third cy cle. Al ter nat ing dolostones and black dolomitic mudstones form the third cy cle, which is 17 m thick. The Up per Tri as sic de pos its are eroded and cov ered by the Lower Ju ras sic sed i ments (Fig. 2; Kotañski, 1956b). Both abrupt fa cies changes and seis mically-gen er ated slumps in di cate that sed i men tary en vi ron ment in the Tatri-cum Ba sin in the lat est Ladinian–Norian time was con trolled by block tec tonic move ments. It cor re sponds to tec -tonic move ments of the Labinian phase (Kotañski, 1956b, 1961). Horsts were eroded or ex posed to pedogenic pro -cesses while in troughs red bed or salt-marsh sed i ments were de pos ited. Rise of tec tonic blocks was caused by dis in te gra tion of the south ern edge of the NorthEu ro pean Plat -form due to ex is tence of mega-shear faults zone in the Penninic Rift (Michalík, 1993, 1994).

PRO DUC TIV ITY AND SOURCE OF OR GANIC MAT TER

Both low TOC con cen tra tion (be low 0.04 wt.%) and ab sence of a skel e tal fauna in car bon ates sug gest low pro -duc tiv ity in the ba sin. Only black dolomitic mudstones do

have higher con cen tra tion of TOC (to 3 wt.%; Ta ble 1). Palyno log i cal ma te rial sug gests ter res trial or i gin of or -ganic mat ter (Annette Götz, pers. commun., 2006).

The con tent of el e men tary sul phur sug gests the pres -ence of orig i nal sed i men tary py rite. Ab s-ence of short-chain al kanes can be an ef fect of the biodegradation of or ganic mat ter (Marynowski et al., 2001). Dom i na tion of long-chain al kanes with un even num ber of C at oms in di cates that they were prob a bly de rived from land plants (Tissot & Welte 1984; Meyers, 1997; Marynowski et al., 2001). This fea ture points to the ter res trial or i gin of or ganic mat ter. More over, pristane ver sus phytane ra tio, about 1, sup ports this con clu sion (Fig. 8; Waleñczak, 1987). The ex clu sive presence of ar o matic hy dro car bons like phenanthrene and methylophenanthrene and ab sence of steranes and hopanes are an in di ca tors of high ther mal ma tu rity of the or ganic mat ter. It is ad di tion ally con firmed by strong ther mal deg ra -da tion of palynological material (Annette Götz, pers. commun., 2006).

CLI MATE CON DI TIONS

Geo chem i cal in di ca tors based on the ra tio of main el e -ments in siliciclastic com po nents of car bon ate rocks in form about palaeoclimate changes. Ti ta nium (Ti) in sed i men tary rocks is ex clu sively terrigenous. There fore, cor re la tion co ef fi cients of Ti against sil ica (Si), alu minium (Al) and po -tas sium (K) amount ing from 0.91 to 1.00 as well as be tween Si, Al and K amount ing from 0.90 to 1.00 (Fig. 9) in di cate con ti nen tal or i gin of siliciclastic com po nents.

Al2O3/SiO2 ra tio informs about con cen tra tion lev els of

quartz ver sus clay min er als. When the value of this pa ram e -ter is be low 0.1 it in di cates quartz-dom i nated siliciclastic com po nents, whereas the value over 0.3 marks dom i na tion

Fig. 9. Cor re la tive graphs of con cen tra tion of se lected main el e ments in the Dol ina Smytnia val ley se quence. High cor re la tion co ef fi -cients in di cate con ti nen tal or i gin of siliciclastic com po nents. A. Ti ver sus Si. B. Ti ver sus Al. C. Ti ver sus K. D. Al ver sus Si. E. Si ver sus K. F. Al ver sus K

of clay min er als (Lintnerová et al., 1988). In the case of dolostones, dolomitic mudstones and dolomitic regoliths, Al2O3/SiO2 is >0.3. The value of dis cussed in di ca tor in

pedogenic lime stones does not ex ceed 0.2 what sug gests more in ten sive con tri bu tion of siliciclastics (Fig. 2).

Po tas sium and alu minium oc cur in clay min er als struc -ture. Illite, clay min eral of Si and K, is formed in hot and dry cli mate with phys i cal-dom i nated weath er ing (cf. Leeder, 1985; Chamley, 1989). On the other hand, kaolinite (clay min eral of Al and Si) is con sid ered as a min eral formed dur -ing pluvialization in hot and hu mid cli mate con di tions (cf. Keller, 1970; Chamley et al., 1997; Œrodoñ, 1999). There -fore, fluc tu a tion of K/Al ra tio re flects changes of cli mate hu mid ity. K/Al in di ca tor is higher, when the cli mate is drier (Reinhardt & Ricken, 2000). K/Al in di ca tor for pedogenic lime stones is higher by about 0.2 if com pared with the Mid dle Tri as sic car bon ates (see Jaglarz, 2007). It in di cates a cli -mate pluvialization dur ing the lat est Ladinian and early Car- nian time. The in creased value of K/Al in di ca tor in the up -per part of the Dol ina Smytnia se quence sug gests cli mate arididity.

Long-last ing cli mate changes were masked by the shortterm cli mate fluc tu a tions. Par tic u larly high were dif -fer ences of K/Al value for dolostones and dolomitic mud-stones (Ta ble 1). Al ter na tion of dolomitic mudmud-stones and dolostones was caused by pe ri odic fluc tu a tions of cli mate hu mid ity un der hot and semi-arid cli mate con di tions. Dolostones were formed dur ing pe ri ods of more in ten sive chem i cal weath er ing, whereas terrigenous sed i ments were de pos -ited dur ing rel a tively dry pe ri ods. Re la tion ship of dolomitic mudstones with dry pe ri ods can sug gest aeolian origin of their terrigenous components.

The Mid dle Tri as sic car bon ate plat form was emerged in the late Ladinian what brought sig nif i cant changes in fa -cies de vel op ment. De vel op ment of car bon ate palaeosols con tain ing quartz-dom i nated siliciclastics and in ten sive chem i cal weath er ing sug gest cli mate pluvialization at the Ladinian/Carnian bound ary. Cli mate pluvialization (Part-nach event) was caused by the vol ca nic ac tiv ity noted in the Al pine-Carpathian do main dur ing the late Ladinian time (cf. Szulc, 2000). Vol ca nic ac tiv ity can be also con firmed by the ex is tence of tuffites in the top of un der ly ing sed i ments (see GaŸdzicki & Lefeld, 1997).

The be gin ning of pure siliciclastic sed i men ta tion of the Carpathian Keuper should be linked with cli mate pluviali-zation pe riod (Reingraben, Raibl or Lunz events) dur ing early Carnian times. The Al pineCarpathian area was cov -ered by siliciclastic sed i ments at that time (see Lein, 1987; Kovács, 1984; Sauer et al., 1992; Haas et al., 1995; Rüffer & Bechstädt, 1998). Af ter this pe riod, the arid ity of cli mate fol lowed. Geo chem i cal pa ram e ters in di cate the re turn of phys i cal weath er ing, which re sulted in de tri tal com po nents of car bon ates. They are dom i nated by illite which is an in di -ca tor of arid cli mate con di tions. Michalík (1993) and Haas

et al. (1995) also pos tu lated the cli mate aridization in late

Carnian–Norian time. Arid cli mate con di tions re sulted in sig nif i cant re duc tion of siliciciclastic de po si tion in the southern parts of the Al pine-Carpathian re gion (see Kozur & Mock, 1997; Feist-Burkhardt et al., 2008; Rychliñski, 2008).

CON CLU SIONS

1. Sed i men ta tion of the uppermost Ladinian–Norian de pos its from the Dol ina Smytnia val ley was con trolled by two ba sic fac tors: block tec tonic move ments and cli mate changes. Fa cies di ver sity of the Carpathian Keuper sed i ments re sulted from synsedimentary block tec tonic move -ments.

2. Pedogenic lime stones (si lici fied dur ing rel a tively early diagenesis) were formed at the Ladinian/Carnian bound ary in the re sult of the emersion of the Mid dle Tri as -sic car bon ate plat form. For ma tion of pedogenic lime stones took place dur ing the pe riod of cli mate pluvialization in the lat est Ladinian to early Carnian time.

3. Early-diagenetic dolostones and dolomitic mudstones were formed in salt marshes. Salt marshes were pe ri od i cally emerged and in ten sively evap o rated, but strongly in -flu enced by fresh-wa ter. Salt marshes were de vel oped in troughs com mu ni cated with the sea. When troughs were isolated from the sea pure flu vial siliciclastics were depo-sited.

4. Dolostone-dolomitic mudstone com plex from the up per part of Dol ina Smytnia val ley se quence was formed dur ing long-last ing pe riod of cli mate arid ity in up per Car-nian?–Norian time.

5. Dolostone and dolomitic mudstone cou ples rep re -sent short-term fluc tu a tions of cli mate hu mid ity. Dolosto-nes were formed dur ing rel a tively hu mid pe ri ods, whereas dolomitic mudstones dur ing arid periods.

6. Both low TOC con cen tra tion and ab sence of a skel e -tal fauna sug gest low pro duc tiv ity in the ba sin. In ad di tion, com po nents of palynological ma te rial and or ganic com -pounds in di cate a ter res trial or i gin of the organic matter.

Ac knowl edg ments

Kind per mis sion for field work has been pro vided by the Au thor ity of the Tatra Na tional Park in Zakopane. Au thor was sup -ported by MNiSW Grant 2P04D05229 and the Jagiellonian Uni ver sity (DS and BW) funds. I thank Mariusz Rospondek (Jagiellonian Uni ver sity, Kraków) for help ing in geo chem i cal or -ganic anal y ses and Annette Götz (Technische Universität Darm-stadt, Ger many) for pre lim i nary palynological in ves ti ga tion. Joa-chim Szulc (Jagiellonian Uni ver sity, Kraków) is thanked for the in tro duc tion to the study area and fur ther com ments on the in ter pre ta tion of the sed i ments. I thank Krzysztof Strelau for the lan -guage im prove ment of the manu script. I would like to thank revie-wers Jozef Michalík (Slo vak Acad emy of Sci ence, Bratislava) and Tadeusz Peryt (Pol ish Geo log i cal In sti tute, Warszawa) for their crit i cal and help ful com ments.

REF ER ENCES

Aigner, T. & Bachmann, G. H., 1989. Dy namic stra tig ra phy of an evaporite–to–red bed se quence, Gipskeuper (Tri as sic), south -west Ger man Ba sin. Sed i men tary Ge ol ogy, 62: 5–25. AlJuboury, A. I. & Duroviè, V., 1992. Paleoenvironment in ter

-pre ta tion of the Carpathian Keuper rocks as re vealed by clay min eral anal y sis. Geologica Carpathica – Se ries Clays, 2: 73–76.

thian Keuper dolostones. Mineralia Slovaca, 28: 12–20. Álvaro, J. J., Rouchy, J. M., Bechstädt, T., Boucot, A., Boyer, F.,

Debrenne, F., Moreno-Eiris, E., Perejón, A. & Vennin, E., 2000. Evaporitic con straints on the south ward drift ing of the west ern Gond wana mar gin dur ing Early Cam brian times. Palaeo ge ogra phy, Palaeoclimatology, Palaeo ec ol ogy, 160: 105–122.

Andrusov, D., Bystrický, J. & Fusán, O. 1973. Out line of the struc -ture of the West Carpathians. In tro duc tory Ex cur sion Guidebook. X Con gress of CarpathianBal kan Geo log i cal As so ci a -tion. Geologický Ústav Dionýza Štúra, Bratislava, 45 pp. Aziz, H. A., Sanz-Rubio, E., Calvo, J. P., Hilgen, F. J. &

Krijgsman, W., 2003. Palaeoenvironmental re con struc tion of mid -dle Mio cene al lu vial fan to cy clic shal low lac us trine deposi-tional sys tem in the Calatayud Ba sin (NE Spain). Sedimento-logy, 50: 211–236.

Bac-Moszaszwili, M., Burchart, J., G³azek, J., Iwanow, A., Jaro-szewski, W., Kotañski, Z., Lefeld, J., Mastella, L., Ozimkow-ski, W., Roniewicz, P., SkupiñOzimkow-ski, A. & Westwalewicz-Mogilska, E., 1979. Geo log i cal map of the Pol ish Tatra Mountains, 1:30000. Wydawnictwa Geologiczne, Warszawa. Bochwic, B., 1975. Preparatyka organiczna. (In Pol ish).

Wydaw-nictwa Naukowe, Warszawa, 764 pp.

Chafetz, H. S. & Zhang, J., 1998. Authigenic euhedral megaquartz crys tals in a Qua ter nary do lo mite. Jour nal of Sed i men tary Re -search, 68: 994–1000.

Chamley, H., 1989. Clay Sedimentology. Springer, Berlin, 623 pp. Chamley, H., Proust, J. -N., Mansy, J. -L. & Boulvain, F., 1997.

Diagenetic and palaeogeographic sig nif i cance of clay, car bon ate and other sed i men tary com po nents in the mid dle De -vo nian lime stone of west ern Ardenne, France. Palaeogeo-graphy, Palaeoclimatology, Palaeo ec ol ogy, 129: 369–385. Dumont, T., Wieczorek, J. & Bouillin, J. P., 1996. In verted Me so

-zoic rift struc tures in the Pol ish West ern Carpathians (High-Tatric units). Com par i son with sim i lar fea tures in the West ern Alps. Eclogae Geologicae Helvetiae, 89: 181–202.

Feist-Burkhardt, S., Götz, A. E., Szulc, J., Borkhataria, R., Geluk, M., Haas, J., Hornung, J., Jor dan, P., Kempf, O., Michalík, J., Nawrocki, J., Reinhardt, L., Ricken, W., Röhling, H. -G., Rüffer, T., Török, Á. & Zühlke, R., 2008. Tri as sic. In: McCann, T. (ed.), The Ge ol ogy of Cen tral Eu rope. Vol ume 2: Me so zoic and Ce no zoic. Geo log i cal So ci ety, Lon don, pp. 749–821.

Fija³kowska, A. & Uchman, A., 1993. New data on palynology of the Tri as sic nof the Pol ish Tatra Mts. (In Pol ish, Eng lish sum -mary). Przegl¹d Geologiczny, 41: 373–375.

Folk, R. L. & Land, L. S., 1975. Mg/Ca ra tio and sa lin ity: Two con trols over crys tal li za tion of do lo mite. Amer i can As so ci a -tion of Petroelum Ge ol o gists Bul le tin, 59: 60–68.

Fried man, G. M. & Shukla, V., 1980. Sig nif i cance of authigenic quartz euhedra af ter sul fates: Ex am ple from the Lockport For ma tion (Mid dle Si lu rian) of New York. Jour nal of Sed i -men tary Pe trol ogy, 50: 1299–1304.

GaŸdzicki, A. & Lefeld, J., 1997. Pokrywa osadowa. Seria wier-chowa. Trias. Trias dolny (kampil) œrodkowy. (In Pol ish). In: Lefeld, J. & GaŸdzicki, A. (eds), Przewodnik 68 Zjazdu Pols-kiego Towarzystwa Geologicznego, 2–4 paŸdziernika 1997, Zakopane. Polskie Towarzystwo Geologiczne, Warszawa, pp. 46–48.

Haas, J., Kovács, S. & Török, Á., 1995. Early Al pine shelf evo lu -tion in the Hun gar ian seg ments of the Tethys mar gin. Acta Geologica Hungarica, 38: 95–110.

Hardie, L. A., 1987. Per spec tives dolomitization: A crit i cal view of some cur rent views. Jour nal of Sed i men tary Pe trol ogy, 57: 166–183.

Hoefs, J., 1997. Sta ble Iso tope Geo chem is try. Springer, Berlin, 201 pp.

Hud son, J. D., 1977. Sta ble iso topes and lime stone lithification. Jour nal of the Geo log i cal So ci ety, 133: 637–660.

Jaglarz, P., 2007. Evo lu tion of the Tatricum Ba sin in late Olenekian–Norian time in the Pol ish Tatra Mts. (In Pol ish, Eng lish sum mary). Un pub lished Ph. D The sis, Jagiellonian Uni -ver sity, Kraków, 188 pp.

Jaglarz, P. & Rychliñski, T., 2005. Struktury wynurzeniowe w utworach triasu jednostki wierchowej i kri¿niañskiej Tatr. (In Pol ish). Przegl¹d Geologiczny, 53: 880–881.

Jaglarz, P. & Szulc, J., 2003. Mid dle Tri as sic evo lu tion of the Tatricum sed i men tary ba sin: an at tempt of se quence stra tig ra -phy to the Wierchowa Unit in the Pol ish Tatra Mts. Annales Societatis Geologorum Poloniae, 73: 169–182.

Keller, W.D., 1970. Evironmental as pects of clay min er als. Jour -nal of Sed i men tary Pe trol ogy, 40: 788–813.

Korte, C., Kozur, H. W. & Veizer, J., 2005. d13C and d18O val ues of Tri as sic brachi o pods and car bon ate rocks as prox ies for co -eval sea wa ter and paleotemperature. Palaeo ge ogra phy, Pala- eoclimatology, Palaeo ec ol ogy, 226: 287–306.

Kotañski, Z., 1956a. O triasie wierchowym w Tatrach. (In Pol ish). Przegl¹d Geologiczny, 4: 319–323.

Kotañski, Z., 1956b. Strati graphic and palaeogeographic prob lems in the High-Tatric Keuper. (In Pol ish, Eng lish sum mary). Acta Geologica Polonica, 6: 273–286.

Kotañski, Z., 1959a. HighTatric Tri as sic. (In Pol ish, Eng lish sum -mary). Biuletyn Instytutu Geologicznego, 149: 143–157. Kotañski, Z., 1959b. Strati graphi cal sec tion of the HighTatric se

-ries in the Tatra Mts. (In Pol ish, Eng lish sum mary). Biuletyn Instytutu Geologicznego, 139: 7–139.

Kotañski, Z., 1959c. Stra tig ra phy, sedimentology and paleogeo-graphy of the high-tatric Tri as sic in the Tatra Mts. Acta Geo-logica Polonica, 9: 113–145.

Kotañski, Z., 1961. TéctogenÀse et re con sti tu tion de la paléogéo-graphie de la zone Haut-Tatrique dans les Tatras. (In Pol ish, French sum mary). Acta Geologica Polonica, 11: 186–476. Kotañski, Z., 1979a. On the Tri as sic of the Tatra Mts. (In Pol ish,

Eng lish sum mary). Przegl¹d Geologiczny, 27: 369–377. Kotañski, Z., 1979b. The po si tion of the Tatra Mts in the West ern

Carpathians. (In Pol ish, Eng lish sum mary). Przegl¹d Geolo-giczny, 27: 359–369.

Kovács, S., 1984. North Hun gar ian Tri as sic fa cies types: A re -view. Acta Geologica Hungarica, 27: 251–264.

Kozur, H., 1991. The evo lu tion of the Meliata-Hallstatt ocean and its sig nif i cance for early evo lu tion of the East ern Alps and West ern Carpathians. Palaeo ge ogra phy, Palaeoclimatology, Palaeo ec ol ogy, 8: 109–135.

Kozur, H. & Mock, R., 1997. New paleogeographic and tec tonic in ter pre ta tions in the Slovakian Carpathians and their im pli -ca tions for cor re la tions with the East ern Alps and other parts of the West ern Tethys. Part II: In ner West ern Carpathians. Mineralia Slovaca, 29: 164–209.

Leeder, M. R., 1985. Sedimentology. Pro cess and Prod uct. George Allen & Unwin, Lon don, 344 pp.

Lein, R., 1987. Evo lu tion of the North ern Cal car e ous Alps dur ing Tri as sic times. In: Flügel, H. W. & Faupl, P. (eds), Geodyna-mic of the East ern Alps. Deuticke, Vi enna, pp. 85–102. Lintnerová, O. & Hladíková, J., 1992. Dis tri bu tion of sta ble O and

C iso topes and microelements in Tri as sic lime stones of the Veterlín Unit, the Malé Karpaty Mts: their diagenetic in ter -pre ta tion. Geologica Carpathica, 43: 203–212.

Lintnerová, O., Masaryk, P. & Martiny, E., 1988. Trace el e ments dis tri bu tion in Tri as sic car bon ates from Veterník and Havra-nica nappes (the Malé Karpaty Mts). Geologický Zbornik –

Geologica Carpathica, 39: 301–322.

Liu, B., Phillips, F. M. & Camp bell, A. R., 1996. Sta ble car bon and ox y gen iso topes of pedogenic car bon ates, Ajo Moun -tains, south ern Ar i zona: im pli ca tions for paleoenvironmental change. Palaeo ge ogra phy, Palaeoclimatology, Palaeo ec ol -ogy, 124: 233–246.

£uczyñski, P., 2001. De vel op ment his tory of Mid dle Ju ras sic nep tu nian dykes in the HighTatric se ries, Tatra Moun tains, Po -land. Acta Geologica Polonica, 51: 237–252.

Marynowski, L., Gawêda, A., Cebulak, S. & Jêdrysek, M., 2001. Hy dro car bons mi gra tion in tec tonic zones of the West ern Tatra Moun tains crys tal line base ment (Cen tral West ern Car-pathians). Geologica Carpathica, 52: 3–14.

McBride, E. F., 1974. Sig nif i cance of color in red, green, pur ple, ol ive, brown, and grey beds of Difunta Group, north east ern Mex ico. Jour nal of Sed i men tary Pe trol ogy, 44: 760–773. Meyers, P. A., 1997. Or ganic geo chem i cal prox ies of

paleoceano-graphic, paleolimnologic and paleoclimatic pro cesses. Or -ganic Geo chem is try, 27: 213–250.

Michalík, J., 1993. Me so zoic ten sional bas ins in the Al pine-Carpathian shelf. Acta Geologica Hungarica, 36: 395–403. Michalík, J., 1994. Notes on the paleogeography and

paleotec-ton ics of the West ern Carpathian area dur ing the Me so zoic. Mitteilungen der Österreichischen Geologischen Gesell-schaft, 86: 101–110.

Michalík, J., Planderová, E. & Sýkora, M., 1976. To the strati graphic and paleogeographic po si tion of the Tomanová For -ma tion in the up per most Tri as sic of the West Carpathians. Geologický Zbornik – Geologica Carpathica, 27: 299–318. Michalík, J., Kátlovský, V. & Hluštík, A., 1988. Plant re mains in

the Tomanová For ma tion (up per most Tri as sic, West Carpa-thians): their or i gin, com po si tion and diagenetic al ter ation. Geologický Zborník – Geologica Carpathica, 39: 523–537. Moore, C. H. & Druckman, Y., 1981. Burial diagenesis and po ros

-ity evo lu tion, Up per Ju ras sic Smackover, Ar kan sas and Luisiana. Amer i can As so ci a tion of Pe tro leum Ge ol o gists Bul le -tin, 65: 597–628.

Muir, M., Lock, D. & Von Der Borch, C., 1980. The Coorong model for penecontemporaneous do lo mite for ma tion in the mid dle Pro tero zoic McArthur Group, North ern Ter ri tory, Aus tra lia. In: Zenger, D. H, Dun ham, J. B. & Ethington, R. L. (eds), Con cepts and mod els of dolomitization. So ci ety of Eco nomic Pa le on tol o gists and Min er al o gists, Spe cial Pub li ca -tion, 28: 51–67.

Palmer, A. N., 1995. Geo chem i cal mod els for the or i gin of mac ro -scopic so lu tion po ros ity in car bon ate rocks. In: Budd, D. A., Saller, A. H. & Har ris, P. M. (eds), Un con formi ties and Po ros ity in Car bon ate Strata. Amer i can As so ci a tion of Pe tro -leum Ge ol o gists, Mem oir, 63: 77–101.

Passendorfer, E., 1961. Évolution paléogéographique des Tatras. (In Pol ish, French sum mary). Rocznik Polskiego Towarzy-stwa Geologicznego, 30: 351–387.

Peryt, T. M. & Magaritz, M., 1990. Gen e sis of evaporiteas so ci -ated plat form dolomites: case study of the Main Do lo mite (Zechstein, Up per Perm ian), Leba el e va tion, north ern Po land. Sedimentology, 37: 745–761.

Peryt, T. M. & Scholle, P. A., 1996. Re gional set ting and role of me te oric wa ter in do lo mite for ma tion and diagenesis in an evaporite ba sin: stud ies in the Zechstein (Perm ian) de pos its of Po land. Sedimentology, 43: 1005–1023.

Platt, N. H., 1989. Lac us trine car bon ates and pedogenesis: sedi-mentology and or i gin of palustrine de pos its from the Early Cre ta ceous Rupelo For ma tion, W Cameros Ba sin, N Spain. Sedimentology, 36: 665–684.

Raciborski, M., 1891. Flora retycka w Tatrach. (In Pol ish).

Roz-prawy Akademii Umiejêtnoœci, 21: 243–260.

Radwañski, A., 1959. Lit to ral struc tures (cliff, clastic dikes and veins, and bor ings of Potamilla) in the High-Tatric Lias. (In Pol ish, Eng lish sum mary). Acta Geologica Polonica, 9: 231– 280.

Radwañski, A., 1968. Pet ro graph i cal and sedimentological stud ies of the High-Tatric Rha etic in the Tatra Moun tains. (In Pol ish, Eng lish sum mary). Studia Geologica Polonica, 25: 3–146. Reinhardt, L. & Ricken, W., 2000. The strati graphic and geo chem

-i cal re cord of Playa Cy cles: mon -i tor -ing a Pangean mon soonlike sys tem (Tri as sic, Mid dle Keuper, S. Ger many). Palaeo -ge ogra phy, Palaeoclimatology, Palaeo ec ol ogy, 161: 205– 227.

Rospondek, M. J., de Leeuw, J. W., Baas, M., van Bergen, P. F. & Leereveld, H., 1994. The role of or gan i cally bound sul phur in stratiform ore sul phide de pos its. Or ganic Geo chem is try, 21: 1181–1191.

Rospondek, M. J., Marynowski, L., Chachaj, A. & Góra, M., 2009. Novel aryl polycyclic ar o matic hy dro car bons: Phenylphe-nanthrene and phenylanthracene iden ti fi ca tion, oc cur rence and dis tri bu tion in sed i men tary rocks. Or ganic Geo chem is try, 40: 986–1004.

Rüffer, T. & Bechstädt, T., 1998. Tri as sic se quence stra tig ra phy in the west ern part of the North ern Cal car e ous Alps (Aus tria). In: de Graciansky, P.-C., Hardenbol, J., Jacquin, T. & Vail, P. R. (eds), Me so zoic and Ce no zoic Se quence Stra tig ra phy of Eu ro pean Bas ins. So ci ety for Sed i men tary Ge ol ogy, Spe cial Pub li ca tion, 60: 751–761.

Rychliñski, T., 2008. Fa cies de vel op ment and sed i men tary en vi -ron ments of the Carpathian Keuper de pos its from the Tatra Moun tains, Po land and Slovakia. Annales Societatis Geolo-gorum Poloniae, 78: 1–18.

Sarin, D. D., 1962. Cy clic sed i men ta tion of pri mary do lo mite and lime stone. Jour nal of Sed i men tary Pe trol ogy, 32: 451–471. Sauer, R., Seifert, P. & Wessely, G., 1992. Guide book to Ex cur

-sions in the Vi enna Ba sin and the Ad ja cent Al pine-Carpa-thian Thrustbelt in Aus tria. Mitteilungen der Österreichi-schen GeologiÖsterreichi-schen Gesellschaft, 85: 3–239.

Scholle, P. A., Ulmer, D. S. & Melim, L. A., 1992. Latestage cal -cites in the Perm ian For ma tion and its equiv a lents, Del a ware Ba sin mar gin, west Texas and New Mex ico: ev i dence for replecement of pre cur sor evaporites. Sedimentology, 39: 207– 234.

Schreiber, B. C. & El Tabakh, M., 2000. De po si tion and early al -ter na tion of evaporites. Sedimentology, 47 (suppl. 1): 215– 238.

Shinn, E. A., 1968. Prac ti cal sig nif i cance of birds eye struc tures in car bon ate rocks. Jour nal of Sed i men tary Pe trol ogy, 38: 215– 223.

Sonnenfeld, P., 1992. Gen e sis of ma rine evaporites – A sum ma -tion. Geologica Carpathica, 43: 259–274.

Spötl, C. & Burns, S. J., 1991. For ma tion of 18Ode pleted do lo -mite within a ma rine evaporitic se quence, Tri as sic Reichen-hall For ma tion, Aus tria. Sedimentology, 38: 1041–1057. Summer field, M. A., 1983. Pe trog ra phy and diagenesis of silcrete

from the Kalahari Ba sin and Cape coastal zone, south ern Af -rica. Jour nal of Sed i men tary Pe trol ogy, 53: 895–909. Szulc, J., 1993. Early al pine tec ton ics and lithofacies suc ces sion in

the Silesian part of the Muschelkalk ba sin. A syn op sis. In: Hagdorn, H. & Seilacher, A. (eds), Muschelkalk. Schöntaler Sym po sium 1991. Goldschneck, Stuttgart, pp. 19–28. Szulc, J., 2000. Mid dle Tri as sic evo lu tion of the north ern

Peri-Tethys area as in flu enced by early open ing of the Peri-Tethys Ocean. Annales Societatis Geologorum Poloniae, 70: 1–48. Œrodoñ, J., 1999. Use of clay min er als in re con struct ing geo log i cal

pro cesses: Re cent ad vances and some per spec tives. Clay Minerals, 34: 27–37.

Tissot, B. P. & Welte, D. H., 1984. Pe tro leum for ma tion and oc -cur rence. Springer, Berlin, 699 pp.

Tucker, M. E. & Wright, V. P., 1990. Car bon ate Sedimentology. Blackwell, Ox ford, 482 pp.

Turnau-Morawska, M., 1953. Kajper tatrzañski, jego petrografia i sedymentologia. (In Pol ish). Acta Geologica Polonica, 3: 33– 102.

Turner, P., 1980. Con ti nen tal Red Beds. De vel op ments in Sedi-mentology, 29. Elsevier, Am ster dam, 562 pp.

Uhlig V., 1897. Die Geologie des Tatragebirges. I. Einleitung und stratigraphischer Theil. Denkschriften der Akademie der Wissenschaften, Wien, Mathematisch-Naturwissenschaftliche Klasse, 64: 643–684.

Veizer, J., 1970. Zonal ar range ment of the Tri as sic rocks of the West ern Carpathians: A con tri bu tion to the do lo mite prob -lem. Jour nal of Sed i men tary Pe trol ogy, 40: 1287–1301.

Veizer, J. & Demoviè, R., 1974. Stron tium as a tool in fa cies anal -y sis. Jour nal of Sed i men tar-y Pe trol og-y, 44: 93–115. Waleñczak, Z., 1987. Geochemia organiczna. (In Pol ish).

Wydawnictwa Geologiczne, Warszawa, 160 pp.

Ward, W. C. & Halley, R. B., 1985. Dolomitization in mix ing zone of near-sea wa ter com po si tion, late Pleis to cene, north east ern Yucatan Pen in sula. Jour nal of Sed i men tary Pe trol ogy, 55: 407–420.

Wójcik, Z., 1959. High-Tatric se ries in the south side of Mt Bobrowiec (West ern Tatra Moun tains). (In Pol ish, Eng lish sum mary). Acta Geologica Polonica, 9: 165–201.

Wright, V. P. & Wil son, R. C. L., 1987. A terra rosa-like paleosol com plex from the Up per Ju ras sic of Por tu gal. Sedimentology, 34: 259–273.

Zejszner, L., 1852. Monograficzny opis wapienia liasowego w Tatrach i w przyleg³ych pasmach karpackich. (In Pol ish). Rocznik Towarzystwa Nauk, Oddzia³ Nauk Przyrodniczych i Lekarskich, 6: 157–343, Kraków.