BEN TO NI TIZED TUF FITES IN THE LOWER EO CENE DE 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 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: mark@ing.uj.edu.pl
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; oliwa@geol.agh.edu.pl
Ci esz kowski, M., Œro doñ, J., Waœkowska- Oliwa, A. & Leœniak, T., 2006. Ben to ni tized tuf fites in the Lower Eo cene de 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 eral com 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 cene flysch rocks of the Sub sile sian Unit. These de pos its crop out in the ¯ywiec tec tonic win dow and in the tec tonic win dows of the Lanck orona – ¯ego cina Struc tural Zone. The ben to ni tized tuf fites, com posed of al most pure dioc 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 age of 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) on the 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 the Li powa beds that con sist mainly of muddy tur bid ites rep re sented by green or green- brownish shales with rare in 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 tigraphic level 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 could proba 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 sian and 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 eral as 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 of the 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 the Hau terivian (Wie ser, 1985). Within the Sub sile sian Unit Wie 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 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) and Skole 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 eral new 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 tions ex ceeds sev eral cen ti me ters, which is un usual in the flysch de 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 eral com 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 were sepa 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 ing main 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 iec Ridge, 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 few thou sands me ters, thick se quences of flysch type sedi ments
were de pos ited. In many cases, the sedi men ta tion of these deep 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 been de vel oped as non- flysch marly de pos its. This fact shows that 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 and north east, the Cre ta ceous and Pa leo gene clas tic de pos its,
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 the Sub 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 gene time, the sedi men ta tion of varie gated de pos its con tin ued up to 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 were folded 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 the ba 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 placed onto the Euro pean plat form. They cov ered the Mio cene mo -lasse de pos its, which filled the Car pa thian Fore deep that was 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 sian Nappe, which is over thrust from the south by the Ma gura and 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 thrust over the Mio cene mo lasse of the Car pa thian Fore deep, and in the east ern sec tor over the Skole Nappe. The de pos its of the 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 ¯ywiec tec tonic win dow situ ated in the south- western part of the Sile sian Nappe. Many tec tonic win dows are grouped in the Lanck orona-¯ego cina Zone, stretched be tween Wadowice town in the west and Rajbrot vil lage in the east. The Sub -sile sian Nappe sedi ments were found be neath the Sile sian Nappe 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 gated shales are usu ally de vel oped as green, green- brownish or oc ca sion ally varie gated – red and green, muddy and clayey shales. 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 sist mainly of clayey shales and mud stones with rare sand stone in ter ca la tions. They have been de scribed as green or brownish shales in the Wiœn iowa tec tonic win dow (Leœniak
et al., 2001), while on the geo logi cal map of the area (Bur
-tan, 1974; Bur -tan, 1978; Bur -tan, 1993), they were grouped to gether with Czer win Sand stones. The same de pos its were de scribed as grey- greenish and varie gated shales (Leœniak & Waœkowska- Oliwa, 2001a; Ci esz kowski et al., 2001) or as 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 cally 0.5–5.0 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 their prop 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 lel lami 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 ent length and thick ness. In some out crops, thin lay ers of grained cal ci tur bid ites (sy der itic car bon ate rocks) ac com -pany the tuf fites.
DE TAILED DE SCRIP TION
OF 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 scribed below.
¯ego cina Zone
The so- called Lanck orona – ¯ego cina Zone forms a com pos ite an ti cli nal tec tonic struc ture built of the Sile sian and 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 partly re moved by the sub se quent ero sion. The Sub sile sian Unit is visi ble in nu mer ous tec tonic win dows of the Sile sian Nappe.
The ¯ego cina Zone (Skoczylas Ciszewska, 1960) rep -re sents the most east ern part of this tec tonic struc tu-re. Two ben ton ized tuf fites set tings have been found there. They occur 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 A
This 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 kawka Creek (Fig. 1). A 5 cm thick tuf fite layer and two ir regu lar streaks can be found in varie gated shales (Fig. 2) of this outcrop.
Ex po sure B
This 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- creamy ben ton ized tuf fites of 1–5 cm thick oc cur in the out crop of grey, clayey shales.
Wiœn iowa Tec tonic Win dow
Nu mer ous high- quality ex po sures have been ob served in the Czer win Creek. Iso lated out crops were also found in the 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 C
Ex 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 bank of 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).
. 2 . gi F sr e ya l eti ff ut f o s n oi t a l a c re t ni hti w st i s o pe d f o s g ol la ci g o l o hti L
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 D
This set ting was found in the Lipnik Creek, 45 m above its first tribu tary in Lipnik vil lage (Fig. 1). Nine thin lay ers of light- creamy tuf fites oc cur in the out crop of grey clayey shales. These lay ers are dis trib uted ir regu larly within the shale sec tion. Their thick ness ranges from 1 mm to 2 cm.
Ex po sure E
This 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 from Gli chow to Pozna chowice. Three white tuf fite lay ers oc cur there within grey- bluish shales with oc ca sional thin- bedded fine- grained sand stone in ter ca la tions (Fig. 2). One of them is 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 of the Outer Car pa thi ans un til now. It is built of white and light- creamy ben ton ized tuf fite with a fine slightly marked par al lel lami na tion. The tuf fite color changes up wards from white, 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 2 cm 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 be found 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 F
Set ting F is lo cated about 350 m up the creek from set -ting E (Fig 1). Grey- greenish shales with nu mer ous 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 cm thick ness oc cur in this sec tion (Fig. 2). Be low them, five thin tuf fite streaks of vari ous thick nesses are visi ble.
Ex po sure G
The 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 three thick est lay ers (10, 7 and 6 cm) are situ ated in the cen tral part of the sec tion (Fig. 2). Some tuf fite lay ers are rusty and some light- gray, but more of them are white or creamy. In gen eral, they are very simi lar to those de scribed above. Thick est, 10 cm tuf fite layer is lami nated in its lower part (Fig. 3 D). It dis plays gen tly in ter leaved white and light- grayish par al lel lami nae. In lower part of the layer, the tuf 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 shadow grow ing up to top. This tuf fite is di rectly un der lain by a layer of sid er itic car bon ate rock of 35 cm thick ness. It is a cal ci tur bid ite with Bouma in ter vals se quence Tabcd, gray when fresh, and yel lowish or rusty on weath ered sur -face.
Ex po sure H
Next 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 4 cm 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 with in ter ca la tions of fine- grained, medium- bedded sand stones.
Ex po sure I
About 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 cur there 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 J
Fol 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 of tuf fites within the shales. Two lay ers of sid er itic car bon ate rock 10 and 14 cm thick also crop out here (Fig. 2).
Lanck orona Zone
Lanck orona Zone (Ksi¹¿kiewicz, 1951a, b) ex tends west of Myœlen ice up to Wadowice. Be tween Myœlen ice and Wadowice the Sub sile sian Unit is ex posed in sev eral tec tonic win dows in the area of Su³kowice, Lanck orona and Kal waria Ze brzy dowska.
Ex po sure K
This 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 few streaks of ben ton ized tuf fites (Fig. 2). Two of tuf fite lay ers are thin (0.5 cm and 2 cm) and the cen tral one is of 12 cm thick ness. The bot tom tuf fite is di rectly un der lain by 20 cm thick 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 is visi 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 the Sile sian Nappe win dows, filled with the de pos its of Sub sile -sian Unit (Geroch & Gradzi ñski, 1955).
Ex po sure L
Set 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 about 1.8 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 from 0.5 cm up to 5 cm (Leœniak & Waœkowska- Oliwa, 2001b) (Figs.2, 3 B). In the cen tral part of this sec tion, 9 cm thick layer of tur biditic lime stone is visi ble, and, at the top of the sec tion, 40 cm thick layer of fine grained sand stone is situ
-ated. Tuf fites are white or creamy and oc ca sion ally gray. Their col ors con trast mark edly with the shales sur -round ing them. At the bases of some tuf fitic lay ers, red, 1–3 mm thick lami nae are visi ble (Fig. 3 D). The tops of tuf fite lay ers are sharply gray ish. This gray color is well visi 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 posed lo cal ity from the Wiœn iowa Tec tonic Win dow. 10 sam ples were in ves ti gated from ex po sures E–I, lo cated in the banks of 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 the pro 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 from these rocks. Bulk rocks were stud ied as side- loaded ran dom prepa ra tions of pow ders, pre pared by wet grind ing in McCrone mill. <0.2 µm frac tions were sepa rated us ing the com 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 saturated form. A Phil ips dif frac to me ter, equipped with a Cu 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 very simi lar, typi cal of the Car pa thian shales of the Sub sile sian Unit (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). smectite is ran domly in ter strati fied and in all shale sam ples con 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 tic of 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. The ma jor clay min eral is pure or al most pure dioc ta he dral smec tite (100–95%S). It is ac com pa nied by a small amount of kao lin ite (Fig. 4: Gli chów 2). Chlo rite is ab sent. Some sam 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 of
illite-smectite %S
Diagnostic
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 Lithology Bulk 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 of crosses 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 mary beam
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 – 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. It is so fine grained that it can be de tected even in <0.2 µm frac 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 or apa tite were re corded in the bulk sam ples. A trace amount of clay frac tion was de tected af ter dis solv ing sid er ite in the course of Jack son treat ment. The com po si tion of the clay frac 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 nate il lite and or dered illite- smectite, with 30%S (more il litic than in the shales). A trace of ana tase was found in the clay frac 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 have been taken from tuf fites as well as from the sur round ing shales. 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 sented mainly by ag glu ti nated forms (Figs 6, 7, 8).
Fre quent oc cur rence of Glo mo spira ge nus is typi cal for the as sem blages from each sam ple. Such mi cro fauna from the Pol ish sec tor of the Outer Car pa thi ans was de scribed as Early 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 eral as 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 most
fre 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 gle
speci mens of typi cal Eo cene spe cies Glo mo spirella bie dai Sam uel, Reo phax elon ga tus Grzy bowski, Reo phax pi lu lifer Brady, Sac cam mi noi des car pa thicus Geroch oc ca sion ally oc cur. Be sides these spe cies, other com mon com po nents of the dis cussed as sem blages in clude: Asche mo cella car pa
-thica (Neagu), Am modis cus div. sp., Am mosphaer oidina pseu 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 sveni
Grad 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 in
the 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 spira div. 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 ous
ben thic fo rams, with Nut tal lides truem pyi (Nut tall) as most com 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 above the 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 of the Glo mo spira div. sp. Zone. The oc cur rence of sin gle speci mens of fora mini fera, typi cal for the Pa leo cene could in di cate a lower part of the Glo mo spira div. sp Zone, or the as sem blages from the Pa leo cene /Eo cene bound ary. On the bound 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 cene and Eo cene spe cies could be taken to gether in the same sam ple. The authors didn’t find traces of re de po si tion in the stud 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 fites in the Sub sile sian Unit took place in the Early Eo cene. The sam ples taken from ben ton ized tuf fites and sur round ing shales 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 the Sub sile sian Unit and oc cur ring in many set tings, have been poorly 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 in the Sub sile sian Unit, oc cur ring in the up per part of green shales and lower part of so called Li powa Beds sensu Nescie ruk (1998) (Lower Eo cene).
It seems that the tuf fites char ac ter ized in this pa per could be equiva lent to the ben to ni tized tuf fites de scribed from the Sub sile sian Unit in ¯ego cina by 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 outcrops
Foraminifera
¯egocina
zone Wiœniowa tectonic window
Lanckorona 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. + +
Ta ble 2 con tin ued
Tuffites outcrops Foraminifera
¯egocina
zone Wiœniowa tectonic window
Lanckorona zone
¯ywiec window
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) + + +
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 drica Glaess 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 sis grzy 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 to the tuf fite level No 11, sensu Wie ser (1985). They form a clearly 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. The authors pro pose to iden tify the sedi men tary com plex with de scribed tuf fites as a spe cial cor re la tion level. We sug gest call ing it “the Gli chów Tuf fite Ho ri zon”, be cause the best out 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 fite ho 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 are in ter preted as rep re sent ing the peak of the Early Pa leo gene vol 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 mina specta 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 funda Schnit ker et Tjalsma. SEM scale bar = 100 µm
It is not easy to pin point the ex act lo ca tion of the ac tive vol 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 that oc cur in the Sub sile sian Unit. The nu mer ous, not less than thirty, 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 rarely fine- grained sand stone tur bid ites. The tur bid ites origi nated from low den sity sus pen sion grav ity flows that formed dis -tal fans. Such tur biditic cur rents’ en ergy was quite low, so their 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 tween the 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 Unit of East ern Alps in the An therin sec tion in Aus tria close to Sal zburg (Eg ger et al., 1997; Eg ger et al., 2000). Based on mi cro pa le on to logi cal and pet ro logi cal in ves ti ga tions, these tuf 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 Sea re gion (Eg ger et al., 2000). The west ern most Sub sile sian and the Hel vetic sedi men tary ar eas proba bly were con -nected (Golonka, et al. 2003). Per haps the tuf fites from all these re gions could even tu ally be cor re lated based on de tail litho 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 great number of lay ers and lami nae of py ro clas tic ori gin in the Lower Eo cene de pos its of the Sub sile sian Unit com pletes the list of tuf fite set tings in the Pol ish sec tor of the Outer Car pa thi ans. It is usual that the Car pa thian tuf fites in the flysch sedi men tary suc ces sions form very thin lay ers and lami 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 thicker lay ers reach ing up to 17 cm, i.e. the thick est tuf fite layer known from flysch of the Sub sile sian Unit in Po land. In some out crops sepa rated lay ers of fine cal ci tur bid ites (of sid 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 its with 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 thanks to the rela tively quiet sedi men ta tion, domi nated by 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 tures be low 100°C, ac cord ing to the ap proach of Œro doñ and Clauer (2001). The pres ence of pure smec tite in ben to nites is 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 of dia gene sis in the Sub sile sian Unit, made for the same area by 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 ite than from shale is not easy to ex plain. Per haps fu ture K-Ar dat 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 the Eo cene. Proba bly this min eral re flects more ma fic char ac ter of the pri mary Eo cene pi ro clas tics.
Age ex ami na tions of tuf fite bear ing de pos its are based on 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 age of 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 ment and stra tigraphic po si tion, the tuf fites form a clearly visi ble and 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 from other 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 SEM work and to J. Golonka (Jagiel lo nian Uni ver sity) for most kindly of fered re marks to this text. T. Ma lata and M. Muszyñski kindly re viewed the manu script.
This study was sup ported by grant DS no 11.11.140.159 and grant KBN 3PO4 D 020 22.
Streszc zenie
ZBEN TO NI TYZOW ANE TUFITY
W 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 ¯ywca zlo 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 toku Plus 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 toku Lipnik 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 stewek o 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 znego wy cis kania, nie tworz¹ wtedy regu larnych lamin, lecz wystêpuj¹ w formie smug o nieregu lar nej mi¹¿szoœci i d³ugoœci. War stewki tufi 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¿u wystêpuj¹ 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 wowaæ sub tel nie zaryso wan¹ p³ask¹ laminacjê równo leg³¹ (Fig. 3 D). Tufity wystêpuj¹ w obrêbie poziomu ³up ków zielo nych i pstrych oraz 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 zymi wk³ad kami ci enko³awi cowych, drob nozi arnistych pi askow ców. War stwy z Li powej z³o¿one s¹ g³ównie z brunat nych i zielo nych mu³ow ców i i³ow ców z rzadko wystêpuj¹cymi wk³ad kami pias-kow ców. Du¿a iloœæ nawet bardzo ci en kich wk³adek tufitów mog³a siê zachowaæ dziêki bardzo spoko jnej se dy men tacji mu³owych tur bi dytów de pon ow anych z rozr zed zo nych pr¹dów zawi -esi nowych.
Badaniami mineralogicznymi objêto trzy typy litologiczne ska³: 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 s³abe zaawansowanie diagenezy badanej serii skalnej. Smektytowi to-warzyszy podrzêdny kaolinit, brak jest natomiast chlorytu i illitu. W niektórych próbkach zosta³y stwierdzone œladowe iloœci pirytu lub kalcytu. Charakterystycznym sk³adnikiem bentonitów jest anataz, wystêpuj¹cy we wszystkich próbkach w iloœciach porów-nywalnych z kwarcem. £upki otaczaj¹ce tufity maj¹ sk³ad mine-ralny typowy dla ³upków karpackich (por. Kotarba 2003) minera³ mieszanopakietowy illit-smektyt, illit (mika), kaolinit, chloryt, kwarc, plagioklaz, piryt. (Tab. 1, Fig. 4). Próbki z syderytów s¹ niemal monomineralne. Stwierdzono w nich tylko niewielk¹
domieszkê kwarcu, a tak¿e niewielk¹ iloœæ substancji ilastej, o sk³adzie odmiennym ni¿ w bentonitach i ³upkach (Fig. 5) oraz œladowe iloœci kalcytu i apatytu (Tab. 1).
Wczesnoeoceñski wiek depozycji tufitów zosta³ okreœlony na podstawie analiz autochtonicznych zespo³ów ma³ych otwornic z osadów tufitowych oraz ich otoczenia. Typow¹ cech¹ dla tych zespo³ów jest wystêpowanie otwornic aglutynuj¹cych, którym towarzysz¹ nieliczne formy wapienne (Tab. 2, Figs. 6, 7, 8).
Ze wzglêdu na sk³ad taksonomiczny zespo³y wystêpuj¹ce w bentonitach zosta³y podzielone na 2 grupy:
– zespo³y typowe dla poziomu Glomospira div. sp., dla któ-rych charakterystyczn¹ cech¹ jest liczne wystêpowanie okazów z rodzaju indeksowego, oraz obecnoœæ otwornic powszechnie wy-stêpuj¹cych w eocenie tj. Glomospirella biedai Sam uel, Reophax elongatus 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 jest Nuttallides truempyi (Nuttall), iloœæ otwornic z rodzaju Glomo-psira, Recurvoides oraz Paratrochamminoides jest mniejsza w stosunku do grupy pierwszej.
Opisane w niniejszej pracy tufity, wystêpuj¹ce w dolno-eoceñskich utworach jednostki podœl¹skiej, nale¿¹ do poziomu tufitowego nr 11 sensu Wieser (1985) i mog¹ byæ odpowiednikiem tufitów tego samego wieku, opisywanych z innych stanowisk i jednostek 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 wiek depozycji, podobne wykszta³cenie litologiczne, stwierdzono, ¿e ³upki 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.
