BEN TO NI TIZED TUF FITES IN THE LOWER EO CENE DE POS ITS ... · no. 21 – Lower Oligo cene. The...

Annales Societatis Geologorum Poloniae (2006), vol. 76: 197–214.

BEN TO NI TIZED TUF FITES IN THE LOWER EO CENE DE POS ITSOF THE SUB SILE SIAN UNIT (WEST ERN OUTER CAR PA THI ANS,

PO LAND): LI THOL OGY, STRA TIGRAPHIC PO SI TIONAND MIN ERAL COM PO SI TION

Marek CI ESZ KOWSKI1, Jan ŒRO DOÑ2, Anna WAŒKOWSKA- OLIWA3 & Tadeusz LEŒNIAK3

1 Jagiel lo nian Uni ver sity, In sti tute of Geo logi cal Sci ences, Ole an dry 2a, 30- 063 Kraków Po land,e- mail: [email protected]

2 In sti tute of Geo logi cal Sci ences, Pol ish Acad emy of Sci ences, Senacka 1, 31- 002 Kraków, Po land,e- mail: ndsro don@cyf- kr.edu.pl

3 Uni ver sity of Sci ence and Tech nol ogy - AGH, Fac ulty of Ge ol ogy, Geo phys ics and En vi ron men tal Pro tec tion,De part ment of Gen eral and Mathe mati cal Ge ol ogy Mick iewicza 30, 30- 059 Kraków, Po land;

e- mail: tlesniak@ge olog.geol.agh.edu.pl; [email protected]

Ci esz kowski, M., Œro doñ, J., Waœkowska- Oliwa, A. & Leœniak, T., 2006. Ben to ni tized tuf fites in the Lower Eo cenede pos its of the Sub sile sian Unit (West ern Outer Car pa thi ans, Po land): li thol ogy, stra tigraphic po si tion and min eralcom po si tion. An nales So cie ta tis Ge olo go rum Po lo niae, 76: 197–214.

Ab stract: New oc cur rences of ben to ni tized tuf fites were de scribed from nu mer ous out crops of the Lower Eo ceneflysch rocks of the Sub sile sian Unit. These de pos its crop out in the ¯ywiec tec tonic win dow and in the tec tonicwin dows of the Lanck orona – ¯ego cina Struc tural Zone. The ben to ni tized tuf fites, com posed of al most puredioc ta he dral mot mo ril lo nite, form nu mer ous thin lay ers and lami nae, only oc ca sion ally ex ceed ing 5 cm. The ageof the tuf fites is es ti mated as the Early Eo cene (Glo mo spira div. sp. and Sac cam mi noi des car pa thicus zones) onthe ba sis of fo rami nif eral as sem blages. They oc cur in the up per part of green shales and in the lower part of theLi powa beds that con sist mainly of muddy tur bid ites rep re sented by green or green- brownish shales with rarein ter ca la tions of sand stones. The sedi men tary se quences with the tuf fite in ter ca la tions form a lithos tra tigraphiclevel in the Sub sile sian Unit called in the pres ent pa per “the Gli chów Tuf fite Ho ri zon”. This tuf fite ho ri zon couldproba bly be cor re lated with de pos its of simi lar age con tain ing tuf fites which are known from the Ma gura, Sile sianand Skole nap pes.

Key words: Pol ish Outer Car pa thi ans, Sub sile sian Unit, Early Eo cene, ben to ni tized tuf fites, fo rami nif eralas sem blages.

Manu script re ceived 30 June 2005, ac cepted 18 May 2006

IN TRO DUC TION

Tuf fites have been re ported in sev eral tec tonic units ofthe Pol ish Outer Car pa thi ans. 31 lev els of tuf fites were de -scribed within the sedi men tary se quences younger than theHau terivian (Wie ser, 1985). Within the Sub sile sian UnitWie ser (1985) dis tin guished 4 lev els: no. 5 – Up per Ce no -ma nian, no. 7 – Up per Tu ro nian, no. 11 – Lower Eo cene,no. 21 – Lower Oli go cene.

The lower Pa leo gene py ro clas tic sedi ments were de -scribed from the ¯ego cina sur round ings (Skoczylas- Ciszewska, 1956), Pozna chowice Dolne (Bur tan, 1978) and Las Bachowicki (Ksi¹¿kiewicz, 1956; Lisz kowa, 1959;Wie ser, 1952). Simi lar de pos its of the same age were also

no ticed in the Sile sian (Kosz ar ski & Wie ser, 1960) andSkole Units (Kosz ar ski & Kosz ar ski, 1985; Kot larc zyk,1988; Rajchel, 1990; Rajchel, 1994; Wie ser, 1970).

Dur ing field in ves ti ga tions, the authors found sev eralnew oc cur rences with nu mer ous in ter ca la tions of ben ton -ized tuf fites within the lower Pa leo gene de pos its of the Sub -sile sian Unit. The thick ness of some of these in ter ca la tionsex ceeds sev eral cen ti me ters, which is un usual in the flyschde pos its of the Sub sile sian Unit in the Pol ish Outer Car pa -thi ans. In this con tri bu tion, some new oc cur rences are de -scribed, in clud ing fo rami nif eral stra tigra phy and min eralcom po si tion.

Po si tion and char ac ter is tics of Sub sile sian Unit

The Outer Car pa thian sedi men tary ba sins are char ac ter -ized by marked lat eral fa cies changes that high light com -plex pa leo ge og ra phy, where deep sub sid ing troughs weresepa rated by shal low or even emer gent ge an ti cli nal struc -tures – ridges. From the south to the north the fol low ingmain sedi men tary ba sins and ridges (Ksi¹¿kiewicz, 1972),each with dis tinc tive lithosta tigraphic suc ces sion, are iden -ti fied: the Ma gura Ba sin, the Dukla Ba sin, the Bu kow iecRidge, the Sile sian Ridge, the Sile sian Ba sin, the Sub sile -sian Ridge, and the Skole Ba sin. In the troughs up to a fewthou sands me ters, thick se quences of flysch type sedi ments

were de pos ited. In many cases, the sedi men ta tion of thesedeep- sea de pos its took place be low the lo cal cal cite com -pen sa tion depth (CCD).

The de pos its of the Sub sile sian Se ries are not as thick as those in oth ers Outer Car pa thian units and part of them rep -re sent depo si tion above CCD. Some of them, de pos ited dur -ing the Late Cre ta ceous, Pa leo cene and Eo cene, have beende vel oped as non- flysch marly de pos its. This fact showsthat the Sub sile sian sedi men tary area was rela tively shal -lower and in cluded an ele vated zone, even with some pe ri -odi cally emerg ing parts. The Sub sile sian and Sile sian sedi -men tary ar eas were in ter con nected. To wards the north andnorth east, the Cre ta ceous and Pa leo gene clas tic de pos its,

198 M. CI ESZ KOWKI ET AL.

Fig. 1 Tuf fite ex po sures set tings (sketches af ter: A – Ma lata et al., 1996; B – Skoczylas- Ciszewska, 1960; C – Bur tan, 1978; D – Bur -tan, 1966; Bur tan & Szy makowska, 1966; E – Nowak, 1966; ¯ytko, 1966)

typi cal of the Sile sian Ba sin, were gradu ally re placed in theSub sile sian sedi men tary area; at first by varie gated shales,and even tu ally by the marls. Oc ca sion ally, in the Pa leo genetime, the sedi men ta tion of varie gated de pos its con tin ued upto the end of the Mid dle Eo cene. Later, marls and shales and the Lower Oli go cene Menil ite Beds were de pos ited.

In the Neo gene, the sedi ments fill ing the ba sins werefolded and de tached from their sub stra tum and sev eral up -rooted nap pes were cre ated. The nap pes’ com po si tion par -tially re flects the ori gin of se quences of de pos its within theba sins (Ksi¹¿kiewicz, 1977). Dur ing the fold ing and thrust -ing, the main nap pes were partly dif fer en ti ated and sub di -vided into smaller tec tonic units. The Outer Car pa thian nap -pes thrusted one upon an other, were all to gether dis placedonto the Euro pean plat form. They cov ered the Mio cene mo -lasse de pos its, which filled the Car pa thian Fore deep thatwas formed in front of the north ward ad vanc ing nap pes.The Sub sile sian Nappe un der lies tec toni cally the Sile sianNappe, which is over thrust from the south by the Ma guraand Fore- Magura nap pes. In the west ern sec tor of the Pol ish Car pa thi ans the Sile sian and Sub sile sian nap pes were thrustover the Mio cene mo lasse of the Car pa thian Fore deep, andin the east ern sec tor over the Skole Nappe. The de pos its ofthe Sub sile sian Nappe crop out in the north ern part in a nar -row zone in front of the Sile sian thrust as well as in the nu -mer ous tec tonic win dows. The big gest one is the ¯ywiectec tonic win dow situ ated in the south- western part of theSile sian Nappe. Many tec tonic win dows are grouped in theLanck orona-¯ego cina Zone, stretched be tween Wadowicetown in the west and Rajbrot vil lage in the east. The Sub -sile sian Nappe sedi ments were found be neath the Sile sianNappe in many wells.

Li thol ogy

The pa per de scribes tuf fites oc cur ring within the Lower Pa leo gene de pos its: green and varie gated shales or the Li -powa beds of the Sub sile sian Unit. Green and varie gatedshales are usu ally de vel oped as green, green- brownish oroc ca sion ally varie gated – red and green, muddy and clayeyshales. Rare (up to 15%) in ter ca la tions of fine- grained sand -stone tur bid ites also oc cur there. The Li powa Beds con sistmainly of clayey shales and mud stones with rare sand stonein ter ca la tions. They have been de scribed as green or green- brownish shales in the Wiœn iowa tec tonic win dow (Leœniaket al., 2001), while on the geo logi cal map of the area (Bur -tan, 1974; Bur tan, 1978; Bur tan, 1993), they were groupedto gether with Czer win Sand stones. The same de pos its werede scribed as grey- greenish and varie gated shales (Leœniak& Waœkowska- Oliwa, 2001a; Ci esz kowski et al., 2001) oras Li powa Beds (Nescie ruk, 1998) from the ̄ ywiec tec tonic win dow. In the ex po sures in ves ti gated, the dis cussed tuf -fites form nu mer ous thin lay ers and lami nae typi cally0.5–5.0 cm thick, in the ex treme cases reach ing 10–17 cm.Tuf fites are easy to iden tify mac ro scopi cally, be cause theirprop er ties are very dif fer ent from the sur round ing shales.They are much lighter than shales white or creamy, oc ca -sion ally light grey or pink, and also soft, plas tic, fat touched, and swel ling in wa ter. Thicker lay ers dis play sub tle par al lellami na tion. The lami nae usu ally oc cur in groups. In some

places, shaly sedi ments with tuf fite lami nae are strongly tec -toni cally de formed, mainly folded and duc tily squeezed.The tuf fite lami nae form dis con tinu ous streaks of dif fer entlength and thick ness. In some out crops, thin lay ers of fine- grained cal ci tur bid ites (sy der itic car bon ate rocks) ac com -pany the tuf fites.

DE TAILED DE SCRIP TIONOF SE LECTED OUT CROPS

Twelve se lected, best ex posed and spec tacu lar out crops of the de pos its with ben to ni tized tuf fites are de scribedbelow.

¯ego cina Zone

The so- called Lanck orona – ¯ego cina Zone forms acom pos ite an ti cli nal tec tonic struc ture built of the Sile sianand Sub sile sian nap pes thrust one upon an other and re -folded to gether. The north ern limb of this un du lated an ti cli -nal struc ture is cuted by an in verse fault, up lifted and partlyre moved by the sub se quent ero sion. The Sub sile sian Unit isvisi ble in nu mer ous tec tonic win dows of the Sile sianNappe.

The ¯ego cina Zone (Skoczylas- Ciszewska, 1960) rep -re sents the most east ern part of this tec tonic struc ture. Twoben ton ized tuf fites set tings have been found there. Theyoccur in the val ley of the Plus kawka Creek and its tribu tar -ies in Nowe Ry bie vil lage (Fig. 1).

Ex po sure AThis set ting is lo cated in the left bank of a tribu tary,

about 260 me ters up from its junc tion with the Plus kawkaCreek (Fig. 1). A 5 cm thick tuf fite layer and two ir regu larstreaks can be found in varie gated shales (Fig. 2) of thisoutcrop.

Ex po sure BThis set ting was found in the bank of Plus kawka Creek,

about 60 me ters up the creek from the mouth of the tribu tary de scribed above (Fig. 1). Three thin lay ers of light- creamyben ton ized tuf fites of 1–5 cm thick oc cur in the out crop ofgrey, clayey shales.

Wiœn iowa Tec tonic Win dow

Nu mer ous high- quality ex po sures have been ob servedin the Czer win Creek. Iso lated out crops were also found inthe Foszc zówka and Lipnik Creeks (Fig. 1) (Leœniak et al.,2001). The eight best ex posed lo cali ties in the cen tral part of the Lanck orona – ¯ego cina Zone, in the Wiœn iowa Tec tonic Win dow are de scribed be low.

Ex po sure CEx po sure C is lo cated in the Foszc zówka Creek about

1 km from its junc tion with the Krzy wor zeka Creek (Fig. 1). The 1,5 m long ex po sure of grey clayey shales in the bankof the creek con tains 10 ir regu larly dis trib uted in ter ca la -tions of white tuf fite lay ers of 0.5–3 cm thick ness (Fig. 2).

BEN TO NI TIZED TUF FITES IN THE LOWER EO CENE DEPOSITS 199


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sr eyal eti ffut fo snoi ta la cre tni hti

w st iso ped fo sgol la cigo lohtiL


Fig. 3 Tuf fites: A – in Czer win creek – the thick est layer (17 cm) (Wiœn iowa tec tonic win dow), B, C – in Li powa creek (¯ywiec tec -tonic win dow), D – Sedi men tary struc tures within tuf fite layer (Czer win creek – Wiœn iowa tec tonic win dow)

Ex po sure DThis set ting was found in the Lipnik Creek, 45 m above

its first tribu tary in Lipnik vil lage (Fig. 1). Nine thin lay ersof light- creamy tuf fites oc cur in the out crop of grey clayeyshales. These lay ers are dis trib uted ir regu larly within theshale sec tion. Their thick ness ranges from 1 mm to 2 cm.

Ex po sure EThis set ting is situ ated in Gli chów vil lage, in the right

bank of the Czer win Creek (Fig. 1). The ex po sure of tuf fites is lo cated about 450 m up, the creek from the small bridge,not far from the lo cal fire- station situ ated at the road fromGli chow to Pozna chowice. Three white tuf fite lay ers oc curthere within grey- bluish shales with oc ca sional thin- beddedfine- grained sand stone in ter ca la tions (Fig. 2). One of themis 17 cm thick (Fig. 3 A). It is one of the thick est tuf fite layer de scribed from the Sub sile sian Unit in the Pol ish sec tor ofthe Outer Car pa thi ans un til now. It is built of white andlight- creamy ben ton ized tuf fite with a fine slightly markedpar al lel lami na tion. The tuf fite color changes up wards fromwhite, creamy to more gray ish at the top of the layer. Min -era logi cal data show, that this tuf fite layer is rich in mont -mo ril lo nite (Sa lata et al., 2001). About 20 cm above is a 2cm thick layer of tuf fite and 90 cm up the sec tion 10 cm cal -ci tur bid ite layer is lo cated. 0,3 cm tuf fite lam ina can befound at the top of the car bon ate layer. 5 cm above the car -bon ate layer, there are next two very thin, tec toni cally de -formed tuf fite streaks.

Ex po sure FSet ting F is lo cated about 350 m up the creek from set -

ting E (Fig 1). Grey- greenish shales with nu mer ous thin- bedded, fine- grained sand stone in ter ca la tions crop out there in the bank of the creek. Four lay ers of tuf fites of 1–5 cmthick ness oc cur in this sec tion (Fig. 2). Be low them, fivethin tuf fite streaks of vari ous thick nesses are visi ble.

Ex po sure GThe next ex po sure G is lo cated 50 m up the creek from

the set ting F (Fig. 1). It con tains 12 lay ers of ben ton ized tuf -fites in ter ca lat ing gray an gray- greenish shales with oc ca -sional in ter ca la tions of thin bed ded sand stones. The thick -ness of tuf fite lay ers ranges from 0.5 cm to 10 cm. The threethick est lay ers (10, 7 and 6 cm) are situ ated in the cen tralpart of the sec tion (Fig. 2). Some tuf fite lay ers are rusty andsome light- gray, but more of them are white or light- creamy. In gen eral, they are very simi lar to those de scribedabove. Thick est, 10 cm tuf fite layer is lami nated in its lowerpart (Fig. 3 D). It dis plays gen tly in ter leaved white andlight- grayish par al lel lami nae. In lower part of the layer, thetuf fite is mas sive and is yel lowish at the bot tom. In the up -per part of the layer the lami na tion dis ap pears and the tuf fite be comes more crum bly and white with gray ish shadowgrow ing up to top. This tuf fite is di rectly un der lain by alayer of sid er itic car bon ate rock of 35 cm thick ness. It is acal ci tur bid ite with Bouma in ter vals se quence Tabcd, light- gray when fresh, and yel lowish or rusty on weath ered sur -face.

Ex po sure HNext 90 m up the creek, in its right bank there is lo cated

an other set ting (H) (Fig. 1). Two lay ers of tuf fites (2 and 4cm thick) and two lay ers of sid er itic car bon ate rock (4 and 5 cm thick) (Fig. 2) oc cur here within gray- green shales within ter ca la tions of fine- grained, medium- bedded sand stones.

Ex po sure IAbout 100 m from the set ting H there is an out crop of

shales and tuf fites re sem bling those de scribed in the pre vi -ous out crops (Fig. 1). A few thin sand stone lay ers oc curthere at top of the cropped out sec tion. Within the shales,three lay ers of white tuf fites 1–5 cm thick have been no ticed (Fig. 2).

Ex po sure JFol low ing the sec tion 600 m up the creek, it is pos si ble

to find three thin lay ers 1–3 cm thick and a few streaks oftuf fites within the shales. Two lay ers of sid er itic car bon aterock 10 and 14 cm thick also crop out here (Fig. 2).

Lanck orona Zone

Lanck orona Zone (Ksi¹¿kiewicz, 1951a, b) ex tendswest of Myœlen ice up to Wadowice. Be tween Myœlen iceand Wadowice the Sub sile sian Unit is ex posed in sev eraltec tonic win dows in the area of Su³kowice, Lanck orona and Kal waria Ze brzy dowska.

Ex po sure KThis set ting is lo cated in the Goœci bia Creek about 0.5

km up the dam which is situ ated by the road con nect ing Ja -si enica and Har bu towice vil lages (Fig. 1). There is an out -crop of gray- greenish clayey shales with lay ers and a fewstreaks of ben ton ized tuf fites (Fig. 2). Two of tuf fite lay ersare thin (0.5 cm and 2 cm) and the cen tral one is of 12 cmthick ness. The bot tom tuf fite is di rectly un der lain by 20 cmthick layer of a tur biditic lime stone. 30 cm be low the lime -stone there is an other layer of white tuf fite. The thick est one is creamy or some where rusty in lower part, up ward pass ing steeply to light- gray. Softly marked par al lel lami na tion isvisi ble within this layer. Within the shales above, a few very thin streaks be low a gray col ored tuf fite layer can be seen.

¯ywiec Tec tonic Win dow

¯ywiec Tec tonic Win dow is the big gest among theSile sian Nappe win dows, filled with the de pos its of Sub sile -sian Unit (Geroch & Gradzi ñski, 1955).

Ex po sure LSet ting L is lo cated in the north- western part of the

¯ywiec Tec tonic Win dow in the Li powa vil lage (Fig. 1).There in the left bank of ¯arnówka Creek, crops out about1.8 m long sec tion of gray- green shales in ter ca lated by four -teen thin lay ers of ben ton ized tuf fites of the thick ness from0.5 cm up to 5 cm (Leœniak & Waœkowska- Oliwa, 2001b)(Figs.2, 3 B). In the cen tral part of this sec tion, 9 cm thicklayer of tur biditic lime stone is visi ble, and, at the top of thesec tion, 40 cm thick layer of fine- grained sand stone is situ -


ated. Tuf fites are white or creamy and oc ca sion ally light- gray. Their col ors con trast mark edly with the shales sur -round ing them. At the bases of some tuf fitic lay ers, cherry- red, 1–3 mm thick lami nae are visi ble (Fig. 3 D). The topsof tuf fite lay ers are sharply gray ish. This gray color is wellvisi ble es pe cially in the thick est lay ers.

MIN ERAL COM PO SI TION

Since all de scribed out crops con tain very simi lar rocks,their min eral com po si tion was stud ied in the best ex posedlo cal ity from the Wiœn iowa Tec tonic Win dow. 10 sam pleswere in ves ti gated from ex po sures E–I, lo cated in the banksof Czer win Creek. 4 sam ples rep re sent shales, 4 ben to nites,and 2 Fe- carbonates. Their ap proxi mate po si tions in thepro file are given in Ta ble 1.

All sam ples were stud ied by X- ray dif frac tion (XRD)both as bulk rocks and in <0.2 µm frac tions sepa rated fromthese rocks. Bulk rocks were stud ied as side- loaded ran domprepa ra tions of pow ders, pre pared by wet grind ing inMcCrone mill. <0.2 µm frac tions were sepa rated us ing thecom plete Jack son (1975) pro ce dure, ap plied in or der to dis -

solve car bon ates and re move or ganic mat ter and iron ox -ides. They were stud ied as ori ented prepa ra tions, sedi -mented on glass slides, both in air- dry and eth yl ene glycol- saturated form. A Phil ips dif frac to me ter, equipped with aCu lamp, and a graph ite mono chro ma tor were used.

Mixed- layer illite- smectite and smec tite were iden ti fied in gly co lated prepa ra tions us ing the po si tions of ap pro pri ate pairs of ba sal re flec tions (Œro doñ 1980, 1981, 1984; Dudek& Œro doñ, 1996).

The min eral com po si tion of all shale sam ples is verysimi lar, typi cal of the Car pa thian shales of the Sub sile sianUnit (comp. Ko tarba, 2003): mixed- layer illite- smectite, il -lite + mica, kao lin ite, chlo rite, quartz, pla gio clase, cal cite,and in individual sam ples py rite or ana tase (Tab. 1). Illite- smectite is ran domly in ter strati fied and in all shale sam plescon tains ca. 50%S (smec tite lay ers; Fig. 4: Gli chów 1).

The com po si tion of ben to nite sam ples is char ac ter is ticof al tered py ro clas tics: a very low amount of quartz, the lack of dioc ta he dral mica, and the pre domi nance of clay. Thema jor clay min eral is pure or al most pure dioc ta he dralsmec tite (100–95%S). It is ac com pa nied by a small amountof kao lin ite (Fig. 4: Gli chów 2). Chlo rite is ab sent. Somesam ples con tain trace amounts of cal cite.


Ta ble 1

Re sults of X- ray dif frac tion ex ami na tion. For illite- smectite and smec tite, po si tions of di ag nos tic peaks are given

Sample Lithology

< 0.2 µm fraction, glycolated

Diagnostic peaks ofillite-smectite

%SDiagnostic

peaks of i-s%S K Ch I Anatase Quartz Apatite

Glichów 1 variegated shale 16.22 31.88 50 + tr + +

Glichów 2 bentonite 15.78 26.46 31.82 96 43.00 48.50 95 + +

Glichów 3 shale between bent. 16.24 31.86 50 + tr + tr

Glichów 4 bentonite 15.80 26.48 31.84 98 43.00 48.58 100 + tr

Glichów 5 bentonite 15.80 26.48 31.80 98 43.00 48.56 100 tr tr

Glichów 6 shale 16.20 26.58 31.88 50 + tr + +

Glichów 7 bentonite 15.78 26.48 31.78 100 42.98 48.52 100 tr tr

Glichów 8 shale 16.26 31.96 50 + tr + +

Glichów 9 siderite layer 16.68 30 +++ ++ tr tr

Glichów 10 siderite concretion 16.70 30 +++ ++ tr +

Sample LithologyBulk rock

K CH I Anatase Calcite Pyrite Quartz Apatite Siderite

Glichów 1 variegated shale + + ++ ++ + +++

Glichów 2 bentonite ++ ++ ++

Glichów 3 shale between bent. + + ++ +++

Glichów 4 bentonite + ++ tr +

Glichów 5 bentonite + ++ tr

Glichów 6 shale + + ++ tr +++

Glichów 7 bentonite + ++ tr tr

Glichów 8 shale + + ++ + +++

Glichów 9 siderite layer tr + ++++

Glichów 10 siderite concretion + + ++++

%S – per cent of smec tite in mixed- layer illite- smectite (for ben to nites % S by two tech niques); K – kao lin ite, CH – chlo rite; I – il lite, tr – trace. Num ber ofcrosses re flects rela tive abun dance of a given min eral.


Fig. 4. Ex am ples of XRD pat terns of gly co lated, ori ented prepa ra tions of <0.2 µm frac tions of a shale (Gli chów 1) and a ben to nite (Gli -chów 2). IS – illite- smectite, I – il lite, K – kao lin ite, Ch – chlo rite, An – ana tase, Al – alu mi num from the Al foil block ing the pri marybeam

Fig. 5. Ex am ples of XRD pat terns of air dry and gly co lated, ori ented prepa ra tions of <0.2 µm frac tion of a car bon ate rock. IS – illite- smectite, I – il lite, Ch – chlo rite, Ap –apa tite, H? – proba bly hal ite, Al – alu mi num from the Al foil block ing the pri mary beam

A char ac ter is tic com po nent of the in ves ti gated ben to -nites, al most ab sent from the sur round ing shales, is ana tase,pres ent in all sam ples in quan ti ties com pa ra ble to quartz. Itis so fine grained that it can be de tected even in <0.2 µmfrac tion (Fig. 4).

The car bon ate sam ples are com posed al most ex clu -sively of sid er ite. Trace amounts of quartz and cal cite orapa tite were re corded in the bulk sam ples. A trace amountof clay frac tion was de tected af ter dis solv ing sid er ite in thecourse of Jack son treat ment. The com po si tion of the clayfrac tion is very dif fer ent from the sur round ing shales (Fig.5), char ac ter ized by domi nant Fe- rich chlo rite, sub or di nateil lite and or dered illite- smectite, with 30%S (more il liticthan in the shales). A trace of ana tase was found in the clayfrac tions from both car bon ate sam ples, as well as some apa -tite in one of them.

FO RA MI NIF ERAL STRA TIGRA PHY

57 sam ples used for the bi os tra tigraphi cal study havebeen taken from tuf fites as well as from the sur round ingshales. Mini mum 3 sam ples from each ex po sure were thor -oughly in ves ti gated. Ta ble 2 pres ents the list of fo rami nif -eral taxa from one typi cal sam ple from each ex po sure. Mi -cro fos sils were sepa rated us ing stan dard mi cro pa le on to logi -cal meth ods. Well pre served fora mini fera are rep re sentedmainly by ag glu ti nated forms (Figs 6, 7, 8).

Fre quent oc cur rence of Glo mo spira ge nus is typi cal forthe as sem blages from each sam ple. Such mi cro fauna fromthe Pol ish sec tor of the Outer Car pa thi ans was de scribed asEarly Eo cene as sem blage (B¹k et al., 1997; Jed norowska,1968; Jurk iewicz, 1967; Ma lata et al., 1996; Mor giel &Olszewska, 1981; Mor giel & Szy makowska, 1978; Waœ-kowska- Oliwa, 2000; Waœkowska- Oliwa & Leœniak,2003). In de pendent Acme Zone Glo mo spira div. sp. dis tin -guished by Olszewska (1997) was used in the bi os tra -tigraphic zo na tion pre sented in this pa per.

Based on taxo nomi cal com po si tion, the fo rami nif eralas sem blages from the tuf fites were di vided into two groups:

– group 1 – as sem blages typi cal for the Glo mo spira div. sp. Zone with nu mer ous ex am ples of Glo mo spira. Glo mo -spira ge nus is rep re sented by 5 spe cies (Tab. 1). The mostfre quent Glo mo spira cha roi des (Jones et Parker) and Glo -mo spira gor dialis (Jones et Parker), taken to gether com pose 70% of the as sem blage. Tu bu lar forms: Rhabdam mina, Rhi -zam mina, Nothia and Re cur voi des div. sp., as well Para tro -cham mi noi des div. sp are also rela tively fre quent. Sin glespeci mens of typi cal Eo cene spe cies Glo mo spirella bie daiSam uel, Reo phax elon ga tus Grzy bowski, Reo phax pi lu liferBrady, Sac cam mi noi des car pa thicus Geroch oc ca sion allyoc cur. Be sides these spe cies, other com mon com po nents ofthe dis cussed as sem blages in clude: Asche mo cella car pa -thica (Neagu), Am modis cus div. sp., Am mosphaer oidinapseu do pau cilo cu lata (Mjat liuk), Gero cham mina con versa(Grzy bowski), Hap lo phrag moi des wal teri (Grzy bowski),Hy peram mina elon gata Brady, Prae cys tam mina sveniGrad stein et Ka min ski, Sac cam mina pla centa (Grzy -bowski), Spi roplec tam mina specta bilis (Grzy bowski),Thal man nam mina sub turbinata (Grzy bowski), Tro cham -

mina div. sp. Poorly pre served cal care ous fo rams oc cur to -gether with ag glu ti nated forms. The ben thic ge nus Nut tal -lides truem pyi (Nut tall) is com mon. The other ben thic fo -rams Abysam mina po agi Schnit ker et Tjalsma, Abysam mina quad rata Schnit ker et Tjalsma, Eponi des sub can didu lus(Grzy bowski), Eponi des um bona tus (Re uss), Den ta lina sp., No dosaria sp., Osan gu laria div. sp., Quad ri mor phina pro -funda Schnit ker et Tjalsma, as well plank tonic forms e.g.Acar in ina, Glo bi gerina, Sub bot ina, spo radi cally oc cur inthe as sem blage. Such as sem blages were found in the ex po -sures A, C, D, E, G, H, L (Fig. 1). The com po si tion of as -sem blages from lo cali ties F, G, H (Fig. 1) is the same as de -scribed above, but the authors no ticed a sin gle oc cur rence(one ex am ple/sam ple) of Rze hak ina fis sis to mata/min ima,Hap lo phrag moi des cf. mjat liu kae (Mas³akowa), and Glo -mo spirella grzy bowskii (Jurk iewicz).

– group 2 – as sem blages of the Sac cam mi noi des car pa -thicus Zone – the speci mens of Glo mo spira, Para tro cham -mi noi des and Re cur voi des ge nus are com mon, but less nu -mer ous than in the as sem blages typi cal for the Glo mo spiradiv. sp. Zone. More fre quent are in dex taxa Sac cam mi noi -des car pa thicus and Reo phax ge nus and also cal care ousben thic fo rams, with Nut tal lides truem pyi (Nut tall) as mostcom mon. In these as sem blages, a sin gle Re ticu lo phrag -mium am plec tens (Grzy bowski) was found. The first oc cur -rences of Re ticu lo phrag mium am plec tens (Grzy bowski)and Reo phax elon ga tus (Grzy bowski) were no ticed abovethe Glo mo spira acme, in the late Early Eo cene (Olszewska,1997). These as sem blages were found in the ex po sures B, J(Fig. 1).

De scribed fo rami nif eral as sem blages bear fea tures ofthe Glo mo spira div. sp. Zone. The oc cur rence of sin glespeci mens of fora mini fera, typi cal for the Pa leo cene couldin di cate a lower part of the Glo mo spira div. sp Zone, or theas sem blages from the Pa leo cene /Eo cene bound ary. On thebound ary be tween the Eo cene and the Pa leo cene the sedi -men ta tion could be con dense, and, there fore, the Pa leo ceneand Eo cene spe cies could be taken to gether in the samesam ple. The authors didn’t find traces of re de po si tion in thestud ied ma te rial there. Taxo nomic com po si tion of fo rami -nif eral as sem blages sug gests that the depo si tion of tuf fitesin the Sub sile sian Unit took place in the Early Eo cene. Thesam ples taken from ben ton ized tuf fites and sur round ingshales dis play simi lar age, but some in di vid ual fea tures dif -fer en ti at ing fora mini fera as sem blages have been ob served.

DIS CUS SION

The Lower Eo cene de pos its, while wide spread in theSub sile sian Unit and oc cur ring in many set tings, have beenpoorly de scribed un til now. This con tri bu tion fills such gap, by char ac ter iz ing the se quence of tuf fite bear ing de pos its inthe Sub sile sian Unit, oc cur ring in the up per part of greenshales and lower part of so called Li powa Beds sensuNescie ruk (1998) (Lower Eo cene).

It seems that the tuf fites char ac ter ized in this pa percould be equiva lent to the ben to ni tized tuf fites de scribedfrom the Sub sile sian Unit in ¯ego cina by Skoczylas- Cieszewska (1956), from Pozna chowice Dolne by Bur tan



Ta ble 2

Oc cur rence of small fora mini fera in tuf fites and sur round ing de pos its

Tuffites outcropsForaminifera

¯egocinazone

Wiœniowa tectonic windowLanckorona

Zone¯yiec

window

A B C D E F G H I J K L

Abysammina poagi Schnitker et Tjalsma + + +

Abysammina quadrata Schnitker et Tjalsma + + +

Acarinina soldadoenis (Brünnimann) +

Acarinina nitida (Martin) +

Acarinina primitiva (Finaly) +

Acarinina sp. + + + +

Ammobaculites sp. + +

Ammodiscus cretaceus (Reuss) + + + + + + + + + +

Ammodiscus incertus (d'Orbigny) + + + + + +

Ammodiscus peruvianus Berry + + + + + + + +

Ammodiscus planus Loeblich + + + + + + + + +

Ammodiscus tenuissimus Grzybowski + + + + + +

Ammolagena clavata (Jones et Parker) + + +

Ammosphaeroidina pseudopauciloculata (Mjatliuk) + + + + + + + + + + +

Anomalina preacuta Vasilenko + +

Anomalina acuta (Plummer) + + +

Arenobulimina dorbignyi (Reuss) + + +

Aschemocella carpathica (Neagu) + + + + + +

Bathisiphon sp. + + + + +

Caudammina ovulum (Grzybowski) + + + + + +

Cibicides sp. + + +

Clinapertina complanata Tjalsma et Lohman +

Dentalina sp. + + +

Ellipsoglandulina sp. + + +

Eponides subcandidulus (Grzybowski) + + +

Eponides umbonatus (Reuss) + + + + +

Eponides sp. + + +

Gavelinella sp. + +

Gerochammina conversa (Grzybowski) + + + + + + + + + + +

Gerochammina lenis (Grzybowski) + + + + + +

Globigerina turgida Finaly +

Globocassidulina inexculpta (Franzenau) +

Glomospira charoides (Jones et Parker) + + + + + + + + + + + +

Glomospira glomerata (Grzybowski) + + + + + +

Glomospira gordialis (Jones et Parker) + + + + + + + + + + + +

Glomospira irregularis (Grzybowski) + + + + + + + +

Glomospira serpens (Grzybowski) + + +

Glomospirella biedai Samuel + + +

Glomospirella grzybowskii (Jurkiewicz) + +

Gyroidinoides sp. +

Haplophragmoides kirki Wickenden + + + +

Haplophragmoides cf. mjatliukae (Mas³akowa) + +

Haplophragmoides porrectus Mas³akowa +

Haplophragmoides walteri (Grzybowski) + + + + + + + +

Hormosina velascoensis (Cushman) + + + + + + +

Hyperammina elongata Brady + + + + + + + + +

Hyperammina gaultina Dam +

Hyperammina sp. + +

Kalamopsis grzybowskii (Dyl¹¿anka) + + + + +


Ta ble 2 con tin ued

Tuffites outcropsForaminifera

¯egocinazone

Wiœniowa tectonic windowLanckorona

zone¯ywiecwindow

A B C D E F G H I J K L

Karrerulina coniformis (Grzybowski) + + + + + +

Karrerulina horrida (Mjatliuk) + + +

Lenticulina sp. +

Lituotuba lituiformis (Brady) + + + + + +

Nodosaria sp. + + + + +

Nonion cf. havanense Cushman et Bermudez +

Nothia excelsa (Grzybowski) + + + + + + + + + + + +

Nuttallides truempyi (Nuttall) + + + + + + +

Osangularia plummerae Brotzen + +

Paratrochamminoides div. sp. + + + + + + + + + + +

Pleurostomella cf. eocena Gümbel + +

Psamminopelta gradsteini Kaminski et Geroch + + +

Pseudonodosaria sp. + +

Psamosphaera sp. + +

Pullenia sp. +

Quadrimorphina profunda Schnitker et Tjalsma + + +

Praecystammina sveni Gradstein et Kaminski + + + + + + + +

Recurvoides div. sp. + + + + + + + + + + + +

Reophax duplex Grzybowski + + + +

Reophax elongatus Grzybowski + + + + + + +

Reophax nodulosus Brady + + + + + + + + +

Reophax pilulifer Brady + + + + + + + + + + + +

Reticulophragmium amplectens (Grzybowski) + +

Rhabdammina div. sp. + + + + + + + + + + + +

Rhizammina indivisa Brady + + + + + + + + + +

Rzehakina fissistomata/minima ? + +

Saccammina grzybowskii (Schubert) + + + + + + +

Saccammina placenta (Grzybowski) + + + + + + + + + + + +

Saccamminoides carpathicus Geroch + + + + +

Spiroplectammina spectabilis (Grzybowski) + + + + + +

Stilostomella sp. +

Subbotina linaperta (Finaly) + + + + +

Subbotina hagni (Gohrbandt) +

Subbotina velascoensis (Cushman) + + +

Subbotina triangularis (White) +

Subbotina sp. +

Subreophax splendidus (Grzyzbowski) + +

Thalmannammina subturbinata (Grzybowski) + + + + + + + + + + + +

Trochammina altiformis Cushman et Renz +

Trochammina globigeriniformis (Jones et Parker) + + + + + +

?Trochammina qadriloba (Grzybowski) + + + + + +

Trochammina sp. +

Trochamminoides coronatus (Brady) + + +

Trochamminoides proteus (Karrer) + +


Fig. 6. Small fora mini fera from tuf fites and sur round ing de pos its. A – Nothia ex celsa (Grzy bowski), B, C – Rhabdam mina cy lin dricaGlaess ner, D – Rhabdam mina cy lin drica Glaess ner and Am mo la gena clavata (Jones et Parker), E – Rhi zam mina in di visa Brady, F – Sac -cam mina pla centa (Grzy bowski), G – Hy peram mina ken mil leri Ka min ski, H, I – Am modis cus cre ta ceus (Re uss), J – Am modis cus tenuis -simus Grzy bowski, K – Glo mo spira serpens (Grzy bowski), L – Glo mo spira glom er ata (Grzy bowski), M – Glo mo spira ir regu laris(Grzy bowski), N, O, P – Glo mo spira cha roi des (Jones et Parker), R – Glo mo spira gor dialis (Jones et Parker). SEM scale bar = 100 µm


Fig. 7. Small fora mini fera from tuf fites and sur round ing de pos its. A – Psam min opelta grad steini Ka min ski et Geroch, B – Kala mop sisgrzy bowskii (Dyl¹¿anka), C, D – Reo phax elon ga tus Grzy bowski, E – Reo phax sca laris Grzy bowski, F – Reo phax pi lu lifer Brady, G –Am mosphaer oidina pseu do pau cilo cu lata (Mjat liuk), H, I – Prae cys tam mina sveni Grad stein et Ka min ski, J, K – Hap lo phrag moi des wal -teri (Grzy bowski), L – Para tro cham mi noi des sp., M – Para tro cham mi noi des con tor tus (Grzy bowski), N – Tro cham mi noi des sp., O, P –Sac cam mi noi des car pa thicus Geroch, R – Re cur voi des with Am mo la gena clavata (Jones et Parker). SEM scale bar = 100 µm

(1978), and from Las Bachowicki (Ksi¹¿kiewicz, 1956;Lisz kowa, 1959; Wie ser, 1952). All those tuf fites be long tothe tuf fite level No 11, sensu Wie ser (1985). They form aclearly visi ble wide spread cor re la tion level in the Sub sile -sian Unit in the Pol ish sec tor of the Outer Car pa thi ans. Theauthors pro pose to iden tify the sedi men tary com plex withde scribed tuf fites as a spe cial cor re la tion level. We sug gestcall ing it “the Gli chów Tuf fite Ho ri zon”, be cause the bestout crops oc cur in the Gli chów Vil lage along Czer win creek(Fig. 1).

We sus pect that the py ro clas tic ma te rial of the tuf fiteho ri zons of the same age from Sile sian (Kosz ar ski & Wie -ser, 1960), as well from the Skole Nappe (Kosz ar ski &Kosz ar ski 1985; Kot larc zyk, 1988; Rajchel, 1990; Rajchel,1994; Wie ser, 1970) could be de rived from the same vol -canic erup tions. Like wise, in the Pa leo cene or Lower Eo -cene varie gated shales from the Ma gura Nappe (Sik ora &Wie ser, 1959a, b), ben to ni tized tuf fites are known and arein ter preted as rep re sent ing the peak of the Early Pa leo genevol canic ac tiv ity (Ksi¹¿kiewicz, 1974).


Fig. 8. Small fora mini fera from tuf fites and sur round ing de pos its. A – Re cur voi des nu cleo lus ( Grzy bowski), B, C – Spi roplec tam minaspecta bilis (Grzy bowski), D – Gero cham mina horrida (Grzy bowski), E – Kar re ru lina con versa (Grzy bowski), F – Are nobu limina dor -bignyi (Re uss), G, H – Nut tal lides truem pyi (Nut tall), I, J – Abysam mina po agi Schnit ker et Tjalsma, K – Quad ri mor phina pro fundaSchnit ker et Tjalsma. SEM scale bar = 100 µm

It is not easy to pin point the ex act lo ca tion of the ac tivevol ca noes dur ing the Early Eo cene that pro duced ashes con -sti tut ing the origi nal ma te rial of the ben ton ized tuf fites thatoc cur in the Sub sile sian Unit. The nu mer ous, not less thanthirty, tuf fite in ter ca la tions, tes tify to the fre quency of erup -tions. So many of them, some even very thin, could be pre -served thanks to the rela tively quiet sedi men ta tion, domi -nated by the depo si tion of thin- bedded mud stone or rarelyfine- grained sand stone tur bid ites. The tur bid ites origi natedfrom low den sity sus pen sion grav ity flows that formed dis -tal fans. Such tur biditic cur rents’ en ergy was quite low, sotheir ero sion ac tiv ity has been mini mal, and com mon in ter -ca la tions of hemi- pelagic clay stone are pre served be tweenthe in di vid ual mud- turbidite lay ers.

Very simi lar de pos its of Early Eo cene age with the in -ter ca la tions of ben ton ized vol canic ashes (the set ting known to Ci esz kowski) were de scribed from the Ul tra hel vetic Unitof East ern Alps in the An therin sec tion in Aus tria close toSal zburg (Eg ger et al., 1997; Eg ger et al., 2000). Based onmi cro pa le on to logi cal and pet ro logi cal in ves ti ga tions, thesetuf fites from the An ther ing sec tion were cor re lated with tuf -fites of the same age of the main ash se ries in the North Seare gion (Eg ger et al., 2000). The west ern most Sub sile sianand the Hel vetic sedi men tary ar eas proba bly were con -nected (Golonka, et al. 2003). Per haps the tuf fites from allthese re gions could even tu ally be cor re lated based on de taillitho logi cal, mi cro pa le on to logi cal, pet ro logi cal and geo -chemi cal in ves ti ga tions.

CON CLU SIONS

Find ing and de scrib ing in the pres ent pa per, such greatnumber of lay ers and lami nae of py ro clas tic ori gin in theLower Eo cene de pos its of the Sub sile sian Unit com pletesthe list of tuf fite set tings in the Pol ish sec tor of the OuterCar pa thi ans. It is usual that the Car pa thian tuf fites in theflysch sedi men tary suc ces sions form very thin lay ers andlami nae, rang ing from a few mil li me ters up to 3 cm. The ex -po sures de scribed by the authors also con tain much thickerlay ers reach ing up to 17 cm, i.e. the thick est tuf fite layerknown from flysch of the Sub sile sian Unit in Po land. Insome out crops sepa rated lay ers of fine cal ci tur bid ites (ofsid er itic com po si tion) ac com pany the tuf fites. These sid er -ites have not been ob served in the Lower Pa leo gene sedi -men tary sec tion of the Sub sile sian Unit be low the de pos itswith tuf fites. The tuf fites oc cur in the shaly sedi ments of the up per part of green shales and/or in the Li powa beds.

Tuf fite lay ers could have been pre served so well thanksto the rela tively quiet sedi men ta tion, domi nated by thin- bedded mud stone or rarely fine- grained sand stone tur bid -ites, de pos ited from low den sity sus pen sion grav ity flows.

The %S in the illite- smectite from shales in di cates early stage of bur ial dia gene sis (the maxi mum pa leo tem pera turesbe low 100°C, ac cord ing to the ap proach of Œro doñ andClauer (2001). The pres ence of pure smec tite in ben to nitesis con sis tent with this con clu sion (comp. Šucha et al.,1993). This re sult con firms the evalua tion of the de gree ofdia gene sis in the Sub sile sian Unit, made for the same areaby Ko tarba (2003).

The domi nance of Fe- chlorite in sid er ites can be ex -plained, as sum ing their early dia ge netic crys tal li za tion, par -tially at least at the ex pense of kao lin ite, in such Fe- rich en -vi ron ment. Lower %S in the illite- smectite from sid er itethan from shale is not easy to ex plain. Per haps fu ture K-Ardat ing will solve this puz zle.

The pres ence of ele vated quan ti ties of ana tase in ben to -nites is un usual. Ana tase is not a min eral com mon in ben to -nites (comp. Grim & Gu ven, 1978). In his study of the Car -pa thian ben to nites K³apyta (1975) noted ana tase only in theEo cene. Proba bly this min eral re flects more ma fic char ac terof the pri mary Eo cene pi ro clas tics.

Age ex ami na tions of tuf fite bear ing de pos its are basedon de tail mi cro pa le on to logi cal in ves ti ga tions of fo rami nif -eral mi cro fauna. These stud ies prove the Early Eo cene ageof the in ves ti gated sedi men tary se quence. The fos sil fo rami -nif eral data shows that as sem blages from tuf fite rich se -quences are typi cal for the bi os tra tigraphic lev els: Glo mo -spira div. sp. or Sac cam mi noi des car pa thicus.

Tak ing into ac count the same li thol ogy, de vel op mentand stra tigraphic po si tion, the tuf fites form a clearly visi bleand wide spread cor re la tion level in the Sub sile sian Unit,called here the Gli chów Tuf fite Ho ri zon. The Lower Eo cene de pos its, in clud ing thin tuf fitic lay ers, are also known fromother main tec tonic units of the Outer Car pa thi ans, e.g. from the Skole, Sile sian and Ma gura nap pes. Per haps these de -pos its are cor relable to the Gli chów Ho ri zon of the Sub sile -sian Unit.

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Ac knowl edg ments

Our thanks go to J. Fa ber (Jagiel lo nian Uni ver sity) for SEMwork and to J. Golonka (Jagiel lo nian Uni ver sity) for most kindlyof fered re marks to this text. T. Ma lata and M. Muszyñski kindlyre viewed the manu script.

This study was sup ported by grant DS no 11.11.140.159 andgrant KBN 3PO4 D 020 22.

Streszc zenie

ZBEN TO NI TYZOW ANE TUFITYW DOL NOEO CEÑSKICH OSADACH JED NOSTKI

PODŒL¥SKIEJ (POL SKIE ZACHOD NIE KAR PATY ZEWNÊTRZNE): LI TOLO GIA, PO ZYCJA

STRATY GRAFIC ZNA I SK£AD MIN ER ALNY

Marek Ci esz kowski, Jan Œro doñ, Anna Waœkowska- Oliwa& Ta deusz Leœniak

W osadach dol no pa leo geñskich jed nostki podœl¹skiej w stre -fie lanckoroñsko- ¿egociñskiej oraz w oknie tek tonic znym ¯ywcazlo kali zow ane zosta³y nowe stano wiska zben to ni tyzow anych tufi- tów (Fig. 1). W niniejszej pracy zami eszc zono charak ter ystykê li -tologiczn¹, min era logiczn¹ oraz bi os traty graficzn¹ ich wy bra nych ods³oniêæ. Strefê ¿eg ociñsk¹ reprezen tuj¹ ods³oniêcia w po tokuPlus kawka w Nowym Ry biu (A i B); okno tek tonic zne Wiœn iowej– ods³oniêcia w po toku Foszc zówka w Wiœn iowej (C ), w po tokuLipnik w Lipniku (D), w po toku Czer win w Gli chowie (E–J);strefê lanck oroñsk¹ – ods³oniêcie w po toku Goœci bia w Ja si enicy(K) oraz okno tek tonic zne ¯ywca – ods³oniêcie w po toku ¯ar-nówka w Li powej (L) (Figs. 1, 2).

W zba danych pro filach tufity wystêpuj¹ w formie war steweko prze ciêt nej mi¹¿szoœci od 0,5 do 5 cm, wyj¹tkowo s¹ to war -stewki grubsze (10–17 cm) (Figs. 2, 3). Miejs cami wk³adki tufi -towe s¹ sil nie zde for mow ane tek tonic znie wskutek plastyc znegowy cis kania, nie tworz¹ wtedy regu larnych lamin, lecz wystêpuj¹w formie smug o nieregu lar nej mi¹¿szoœci i d³ugoœci. War stewkitufi towe s¹ zgru pow ane blisko sie bie, w lic zbie od kilku do kilku-na stu. W bez poœred nim kon tak cie z tufitami lub w ich pobli¿uwystêpuj¹ war stwy peli tyc znych sy derytów o mi¹¿szoœci od 10 do 35 cm (Fig. 2). Tufity s¹ barwy bia³ej lub kre mowej, a czasem jas -no pop ie latej lub ró¿ow awej. Charak teryzuj¹ siê s³ab¹ zwiêz³oœci¹, s¹ t³uste w do tyku, na mokro plastyc zne, pêc zniej¹ce w wodzie.Osad tufi towy jest prze wa¿nie pozbawiony struk tur se dy men ta -cyjnych, jedynie w grubszych war stewk ach mo¿na zaob ser wowaæsub tel nie zaryso wan¹ p³ask¹ laminacjê równo leg³¹ (Fig. 3 D).Tufity wystêpuj¹ w obrêbie poziomu ³up ków zielo nych i pstrychoraz warstw z Li powej. £upki s¹ zie lone i zie lono brunatne, miejs -cami czer wone i zie lone, mu³ow cowe lub ³upki z po je dync zymiwk³ad kami ci enko³awi cowych, drob nozi arnistych pi askow ców.War stwy z Li powej z³o¿one s¹ g³ównie z brunat nych i zielo nychmu³ow ców i i³ow ców z rzadko wystêpuj¹cymi wk³ad kami pias-kow ców. Du¿a iloœæ nawet bardzo ci en kich wk³adek tufitówmog³a siê zachowaæ dziêki bardzo spoko jnej se dy men tacji mu³o-wych tur bi dytów de pon ow anych z rozr zed zo nych pr¹dów zawi -esi nowych.

Badaniami mineralogicznymi objêto trzy typy litologiczneska³: ³upki ilaste, bentonity oraz p³askury i konkrecje syderytowe.Bentonity maj¹ sk³ad przeobra¿onych osadów piroklastycznych,charakterystyczna jest dla nich bardzo ma³a zawartoœæ kwarcu,a bardzo du¿a materia³u ilastego (Fig. 4). Dominuj¹cym mine-ra³em ilastym jest niemal czysty dioktaedryczny smektyt (0 do 5% pakietów illitowych). Nik³y stopieñ illityzacji potwierdza s³abezaawansowanie diagenezy badanej serii skalnej. Smektytowi to-warzyszy podrzêdny kaolinit, brak jest natomiast chlorytu i illitu.W niektórych próbkach zosta³y stwierdzone œladowe iloœci pirytulub kalcytu. Charakterystycznym sk³adnikiem bentonitów jestanataz, wystêpuj¹cy we wszystkich próbkach w iloœciach porów-nywalnych z kwarcem. £upki otaczaj¹ce tufity maj¹ sk³ad mine-ralny typowy dla ³upków karpackich (por. Kotarba 2003) minera³mieszanopakietowy illit-smektyt, illit (mika), kaolinit, chloryt,kwarc, plagioklaz, piryt. (Tab. 1, Fig. 4). Próbki z syderytów s¹niemal monomineralne. Stwierdzono w nich tylko niewielk¹


domieszkê kwarcu, a tak¿e niewielk¹ iloœæ substancji ilastej, osk³adzie odmiennym ni¿ w bentonitach i ³upkach (Fig. 5) orazœladowe iloœci kalcytu i apatytu (Tab. 1).

Wczesnoeoceñski wiek depozycji tufitów zosta³ okreœlony napodstawie analiz autochtonicznych zespo³ów ma³ych otwornicz osadów tufitowych oraz ich otoczenia. Typow¹ cech¹ dla tychzespo³ów jest wystêpowanie otwornic aglutynuj¹cych, którymtowarzysz¹ nieliczne formy wapienne (Tab. 2, Figs. 6, 7, 8).

Ze wzglêdu na sk³ad taksonomiczny zespo³y wystêpuj¹cew bentonitach zosta³y podzielone na 2 grupy:

– zespo³y typowe dla poziomu Glomospira div. sp., dla któ-rych charakterystyczn¹ cech¹ jest liczne wystêpowanie okazów zrodzaju indeksowego, oraz obecnoœæ otwornic powszechnie wy-stêpuj¹cych w eocenie tj. Glomospirella biedai Sam uel, Reophaxelongatus Grzybowski, Reophax pilulifer Brady;

– zespo³y poziomu Saccamminoides carpathicus, gdzie rela-tywnie licznie reprezentowanemu taksonowi indeksowemu towa-rzysz¹ otwornice z rodzaju Reophax, pojedyncze okazy Reticulo-phragmium amplectens (Grzybowski) oraz otwornice wapienne

bentoniczne, w obrêbie których najliczniej reprezentowany jestNuttallides truempyi (Nuttall), iloœæ otwornic z rodzaju Glomo-psira, Recurvoides oraz Paratrochamminoides jest mniejsza wstosunku do grupy pierwszej.

Opisane w niniejszej pracy tufity, wystêpuj¹ce w dolno-eoceñskich utworach jednostki podœl¹skiej, nale¿¹ do poziomutufitowego nr 11 sensu Wieser (1985) i mog¹ byæ odpowiednikiem tufitów tego samego wieku, opisywanych z innych stanowisk ijednostek Karpat fliszowych (Skoczylas-Ciszewska, 1956;Burtan, 1978; Ksi¹¿kiewicz, 1956: Liszkowa, 1959; Wieser, 1952, 1960, 1970; Koszarski, 1985; Koszarski & Wieser, 1960;Koszarski & Koszarski, 1985; Kotlarczyk 1988; Rajchel 1990,1994).

Bior¹c pod uwagê szerokie rozprzestrzenienie, ten sam wiekdepozycji, podobne wykszta³cenie litologiczne, stwierdzono, ¿e³upki z wk³adkami tufitów tworz¹ horyzont szeroko rozprzestrze-niony, wyraŸnie wyodrêbniaj¹cy siê w profilach jednostki pod-œl¹skiej. Autorzy proponuj¹, aby nazwaæ go horyzontem tufito-wym z Glichowa.


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