Lithology of glacial sediments of Sanian-2 (Elsterian-2) stage at Tenczynek Basin, Kraków region, Southern Poland

LITHOLOGY OF GLACIAL SEDIMENTS OF SANIAN-2 (ELSTERIAN-2) STAGE IN TENCZYNEK BASIN, KRAKÓW

REGION, SOUTHERN POLAND

Jacek Rutkowski1, Witold Zuchiewicz2, Andrzej Bluszcz3 & Edeltrauda Helios-Rybicka1,4

1 W ydział Geologii, G eofizyki i O chrony Środow iska A kadem ii G órniczo-H utniczej, 30-059 K raków , al. M ickiew icza 30, e-m ail: rutkow ski@ geolog.geol. agh. edu.pl

Instytut N a u k G eologicznych U niw ersytetu Jagiellońskiego, 30-063 K raków , ul. O łeandry 2A, e-m ail: w itold@ ing. uj. edu.pl

3 Instytut F izyki P o litech n iki Śląskiej, 44-100 Gliwice, ul. K rzyw oustego 2, e-mail: b lu szcz@ zeus.polsl.gliw ice.pl 4 e-m ail: helios@ geol.agh.edu.pl

Rutkowski J., Zuchiew icz W., B luszcz A. & H elios-Rybicka E., . Lithology o f glacial sedim ents o f Sanian-2 (Elsterian-2) stage in Tenczynek Basin, Kraków region, Southern Poland. Ann. Soc. Geol. Polon., 247-265.

A b s tr a c t: The paper deals w ith the lithology o f Quaternary sediments that fill the Tenczynek Basin, Kraków Upland. The basin w as eroded w ithin Carboniferous strata before or during the Elsterian. The basin fill can be subdivided into three com plexes, the m iddle one o f w hich records a nearly complete glacial cycle, represented by glacier advance and standstill during the Elsterian-2 (Sanian-2) glacial stage. Sedim ents o f the low er complex were deposited before or during that stage. Following this deposition, a term inoglacial lake w as formed and became gradually filled w ith glaciolacustrine clays and silts that bear a few intercalations o f diam ictons, some o f them shed by slumps. These sediments compose the middle, strongly disturbed com plex w hich, in turn, is unconformably overlain by periglacial sands o f the upper complex, deposited during a tim e-span comprised between the Sanian and W eichselian. The petrographic composition o f gravels and cobbles, determ ined for a wide spectrum o f grain-size classes, is highly variable due to differentiated exaration and the changeable supply o f extraglacial material.

A b s tr a k t: Artykuł om aw ia litologię osadów czw artorzędowych w ypełniających Kotlinę Tenczynka na zachód od Krakowa. Kotlina została w yerodow ana w skałach karbonu przed lub w trakcie zlodow acenia Sanu-2. Piaski i żwiry dolnego kom pleksu osadow ego pow stały przed zlodow aceniem i w wyniku zatam ow ania odpływu przez lądolód. Następnie doszło do utw orzenia jeziora terminoglacjalnego i sedym entacji osadów glacilim nicznych, z wkładkami diam iktytów o bardzo zm iennym uziam ieniu. O sady te, budujące kompleks środkowy, są silnie zabu­

rzone i przykryte niezgodnie przez peryglacjalne piaski pokrywowe kompleksu górnego, osadzone po zlodow a­

ceniu Sanu. Skład petrograficzny żw irów i głazików w osadach glacjalnych, analizowany dla różnych przedziałów frakcyjnych, je st bardzo zm ienny z uwagi na zróżnicowanie lokalnej egzaracji i zm iany w dostawie materiału ekstraglacjalnego.

Key w o rd s : lithology, petrography, Sanian-2 (Elsterian-2) glacial stage, Quaternary, Tenczynek Basin, Southern Poland.

Manuscript received 27 January 1998, accepted 28 December 1998

INTRODUCTION

T h e p a p e r d eals w ith g la c ia l s e d im e n ts o f S a n ia n -2 (E l­

ste ria n -2 ) age th a t cro p o u t in th e T e n c z y n e k B a sin , K ra k ó w U p la n d , so m e 25 k m w e st o f K ra k ó w (F ig s. 1, 2). T h e se se d im e n ts are c o m p o s e d o f h ig h ly v a ria b le se rie s o f silts, clay s an d d ia m ic to n s, ra re ly sa n d s a n d g ra v e ls. T h e y are u n ­ d e rla in m o stly b y C a rb o n ife ro u s ro c k s a n d o v e rla in b y p e rig la c ia l sands. T h e T e n c z y n e k B a sin p ro v id e s a ra re o p ­ p o rtu n ity in S o u th e rn P o la n d to stu d y a n e a rly c o m p le te se d im e n ta ry re c o rd o f th e a d v a n c e a n d sta n d still o f th e

S an ian -2 ic e sh e e t, th e m o s t e x te n s iv e fro m a m o n g P le isto ­ c e n e ic e s h e e ts in P o la n d a n d th e o n ly o n e w h ic h e n c ro a c h e d u p o n th is area. T h is g la c ia l sta g e is u s u a lly c o rre la te d w ith th e E lste ria n -2 stag e o f th e W e st E u ro p e a n stra tig ra p h ic sc h e m e (cf. L in d n e r, 1991; L in d n e r e t a l., 1998).

S e d im e n ts o f th e S a n ia n -2 sta g e in S o u th e rn P o la n d are p re s e rv e d o n ly lo c a lly d u e to stro n g d e n u d a tio n d u rin g the su b s e q u e n t g la c ia l-in te rg la c ia l stag es. T h e re fo re , th e T e n ­ c z y n e k B asin , w ith a n e a rly 50 m - th ic k Q u a te rn a ry infill,

h as b een c h o se n as a s tu d y area. T h e o n ly o n e e x te n s iv e e x ­ p o su re o f g la c ia l se d im e n ts a n d o v e rly in g p e rig la c ia l san d s in th is a re a is situ a te d o n to p o f an a c tiv e q u a rry o f P e rm ia n dia b a se s at N ie d ź w ie d z ia G ó ra (cf. F igs. 1 -4 ) w h e re Q u a te r­

n a ry d e p o sits, a d o z e n o r so m e tre s th ic k , are a c c e ss ib le in a 2 5 0 -m -lo n g , so u th e rn e x p lo ita tio n w a ll. It is th e m o s t e x te n ­ siv e e x p o su re o f g la c ia l se d im e n ts in S o u th e rn P o la n d w h ic h h as n o t y e t b e e n d e s c rib e d , e x c e p t p re lim in a ry c o n tri­

b u tio n s b y R u tk o w sk i e t al. (1 9 9 3 , 1994). F ro m th e n earb y area, SE o f B ro d la in th e R y b n a D e p re ssio n , tills o v e rla in by a e o lia n san d s h a v e b e e n re p o rte d b y D ż u ły ń sk i (1 9 5 6 ).

MATERIAL AND METHODS

D u rin g fie ld stu d ie s in d iv id u a l e x p o su re s h a v e b een lo g g ed (cf. F ig s. 4 - 1 0 ) a n d d e ta ile d g e o lo g ical m a p p in g o f th e T e n c z y n e k B a sin m a rg in s n e a r L ig u n io w a G ó ra, T en- czy n e k , a n d e a s t o f N ie d ź w ie d z ia G ó ra h as b e e n m a d e (cf.

Figs. 2, 3), s u p p le m e n tin g th e e x is tin g 1:50,000 g e o lo g ical

Fig. 1. Tenczynek Basin versus topography o f K rzeszowice region, west o f K raków, southern part o f the Kraków Upland: A - geological sketch, insert cartoon shows the m axim um extent o f Odranian (Drenthe; O) and Sanian (Elsterian; S) glaciations; location o f Niedźwiedzia Góra quarry shown by asterisk; B - topographic sketch (hatchure denotes glaciolacustrine sediments)

CARPATHIAN FOREDEEP (MIOCENE)

CARPATHIAN FORELAND (PALAEOZOIC-MESOZOIC)

m a p s o f th a t a re a (P lo n c z y n s k i & L o p u sirisk i, 1992).

G e o lo g ic a l settin g o f g la c ia l se d im e n ts h as b e e n d e ­ sc rib e d on th e b asis o f an a n a ly s is o f w e ll- lo g d a ta p e rta in ig to co al an d d ia b a se p ro s p e c tio n . M o re th a n 100 logs o f w ells an d e x c a v a tio n p its h a v e b e e n u se d , h a l f o f th e m d rille d af­

te r th e W o rld W a r II, up to th e 1960s. T h e n u m b e r o f w ells c h an g es from 1 -2 p e r sq. km in th e N E p a rt o f th e B asin, th ro u g h 5 - 6 p e r sq. k m in th e re m a in in g p a rt, to 35 p e r sq.

km in th e q u a rry itself. T h e se w e lls s e rv e d as a b a sis fo r c o n ­ stru c tio n o f a d e ta ile d m a p o f th e s u b - Q u a te m a ry to p o g ra ­ p h y (cf. Fig. 2) an d g e o lo g ic a l c ro s s-se c tio n s (cf. Fig. 3).

S eism ic re fra c tio n a n d re fle c tio n p ro file s h a v e b e e n sh o t b y S lu s a rc z y k (1 9 9 7 ) to d e te rm in e th e b o u n d a ry b e ­ tw e e n Q u a te rn a ry a n d u n d e rly in g s e d im e n ts. S e v e n p ro file s h a v e b e e n a n a ly s e d b y th e u s e o f 2 4 -c h a n n e l T e rra lo c M k 6 , the re su lts b e in g c o m p u te d o n th e b a se o f S e iatrix 3 o r S ex ­ tette sy stem s. A c o m p a riso n b e tw e e n g e o lo g ic a l c ro s s se c ­ tions an d g e o p h y sic a l p ro file s m a k e s th e u n e q u iv o c a l d e te r­

m in a tio n o f g e o lo g ic a l b o u n d a rie s im p o ssib le . T h e se d iffi­

cu lties re s u lt fro m g re a t v a ria b ility in g ra in -s iz e o f Q u a te r­

n ary se d im e n ts, v e ry lim ite d k n o w le d g e on th e v e lo c ity o f p ro p a g a tio n o f e la stic w a v e s w ith in th e s e d e p o sits, an d from to o sm all d iffe re n c e s in v e lo c ity ra n g e s b e tw e e n C a rb o n ife r­

ous a n d Q u a te rn a ry strata.

L a b o ra to ry stu d ie s c o n s is te d o f g ra in -s iz e a n a ly s e s o f silts, clay s, d ia m ic tio n s a n d sa n d -g ra v e lly se d im e n ts (cf.

F ig. 11), p e rfo rm e d on sie v e s fo r g ra v e l a n d sa n d fractio n s.

In the c o u rse o f th e a n a ly s is s a m p le s w e re s u c c e s s iv e ly re ­ d u c e d in size by th e q u a rte rin g m e th o d . F o r silt-c la y e y fra c ­ tio n s, sm a lle r th a n 0.1 m m , th e g ra in -siz e h a s b e e n d e te r­

m in e d u sin g th e S a rto riu s s e d im e n ta tio n w e ig h t. T h e re su lts o b ta in e d b y d iffe re n t te c h n iq u e s h a v e th e n b e e n c o m b in e d to sh o w th e full sp e c tru m o f g ra in -s iz e d is trib u tio n o f d ia m ic to n s (cf. Fig. 11), an d n o t o n ly th a t o f sm a lle r fra c ­ tio n s, as it is c u sto m a ry in th e P o lish lite ra tu re . F ro m se ­ lected sam p les o f silts, c la y s a n d d ia m ic to n s , th e fra c tio n

< 0 .0 0 2 m m h as b e e n s e p a ra te d a n d a n a ly s e d b y X -ra y dif- fra c to m e try in re s p e c t to its q u a lita tiv e m in e ra l c o m p o sitio n . X -ra y d ia g ra m s fo r c la y fra c tio n (< 0 .0 0 2 m m ) se p a ra te d from 4 sam p les h a v e b e e n o b ta in e d b y th e X -ra y d iffra c ­ to m e te r D R O N 3 .0. Q u a lita tiv e a n a ly s is c o n siste d in th e stu d y o f d iffra c to g ra m s re g is te re d fo r s a m p le s o rie n te d due to se d im e n ta tio n fro m s u s p e n sio n o f < 0 .0 0 2 m m fra c tio n , air-d ried and sa tu ra te d w ith e th y le n e g ly c o l.

P a rticu lar a tte n tio n has b e e n p a id to g ra v e ls an d c o b b le s ( c f Fig. 12), se p arated fro m d ia m ic to n s an d o th e r sed i­

m en ts. T h e ir p e tro g ra p h ic c o m p o s itio n h a s b e e n d e te rm in e d fo r sev eral fra c tio n s la rg e r th a n 2 m m , u s in g p h i sc a le . T he resu lts are p re s e n te d in p e r c e n t o f th e n u m b e r o f c la s ts, ta k ­ ing each g ra in -siz e class as 100% . F ro m e a c h c la s s 300 c lasts h a v e b e e n a n a ly s e d , e x c e p t th o s e o f th e la rg e st d ia m e ­ ters (R u tk o w sk i, 1977, 1995). D u e to in s ig n ific a n t a m o u n t o f g ra v e l-siz e c la s ts w ith in so m e d ia m ic to n sa m p le s, th e fo l­

lo w in g se p a ra tio n te c h n iq u e h a s b e e n a p p lie d . C la sts la rg e r th an 32 m m in d ia m e te r h a v e b e e n p ic k e d u p in th e field, w h e re a s th e re m a in in g m a te ria l h as b e e n b ro u g h t to th e la b o ra to ry , th en a ir-d rie d a n d s ie v e d to s e p a ra te 4 - 3 2 m m clasts. T h e sm a lle r-siz e m a te ria l h a s b e e n w e t-s ie v e d . T a k ­ ing into a c c o u n t th e sm all p ro p o rtio n o f c o a rs e -g ra in e d m a ­ terial, larg e, sev eral h u n d re d k ilo g ra m e a c h , s a m p le s h a d to

b e c o lle c te d . F o r in s ta n c e , to o b ta in a s u ffic ie n t n u m b e r o f

< 3 2 m m c la s ts fro m s a m p le 3P , ca. 2 5 0 k g o f d iam icto n m u s t h a v e b e e n siev ed . F o r fra c tio n s <2 m m , th e a m o u n t o f CaCC>3 h as b e e n d e te rm in e d b y th e v o lu m e tric m e th o d (cf.

F ig s. 8 -9 ).

T h e rm o lu m in e sc e n c e d a tin g w a s p e rfo rm e d b y one o f u s (A . B lu sz c z ) at th e G liw ic e T e c h n ic a l U n iv e rs ity on 4 s a m p le s o f silts a n d san d s, c o lle c te d fro m th e e a ste rn p art o f th e N ie d ź w ie d z ia G ó ra e x p o s u re ( c f F igs. 7, 9). E ach tim e q u artz g rain s o f 9 0 - 1 5 0 jam fra c tio n h a v e b e e n an aly sed .

GEOLOGICAL SETTING OF TENCZYNEK BASIN AND ITS

SURROUNDINGS

T he T e n c z y n e k B a s in re p r e s e n ts a d e p re s sio n situ ated so u th o f K rz e sz o w ic e (F ig s. 1, 2), w ith in th e T e n c z y n e k R an g e h o rs t (D ż u ły ń s k i, 1953; G ile w sk a , 1972). T h e basin is fille d w ith Q u a te rn a ry s e d im e n ts a n d its to p o ccu rs at 3 1 0 -2 9 0 m a.s.l. in th e so u th a n d th e w e st, slo p in g to som e 2 7 0 -2 9 0 m a.s.l. in th e n o rth . T h e T e n c z y n e k B asin is d ra in e d m a in ly to th e n o rth b y trib u ta rie s o f th e R u d aw a R iv e r, flo w in g th ro u g h a n d e a s t o f T e n c z y n e k , su b o rd in a- te ly to w a rd s th e S an k a R iv e r in th e S E p a rt a n d th e R u dno R iv e r v alley in th e S W part.

T h e to p o g ra p h y an d g e o lo g ic a l se ttin g o f th e T e n c z y ­ n e k B a sin a n d its s u rro u n d in g s are s h o w n in F ig s. 1 an d 2, an d d e sc rib e d in d etail b y D ż u ły ń sk i (1 9 5 3 ), D o k to ro w ic z - H re b n ic k i (1 9 5 4 ), and P lo n c z y n s k i a n d Ł o p u siń s k i (1992).

T he w e ll-lo g d a ta sh o w th a t th e b a se o f th e b a sin is re la ­ tiv e ly flat, b e in g p la c e d a t 2 3 0 - 2 4 0 m a .s.l., a n d slo p in g to so m e 2 2 0 m a.s.l. in th e SE p a rt o n ly (F ig s. 2, 3). Ju d g in g fro m the p re - Q u a te m a ry to p o g ra p h y (F ig . 2), th e b asin w as in itia lly d ra in e d so u th -e a stw a rd s, to w a rd th e p re s e n t S anka R iv e r v a lle y an d , p o ss ib ly , a lso so u th -w e s tw a rd s , to the v a l­

ley o f R u d n o .

T h e c e n tra l p a rt o f th e b a sin re v e a ls a m in o r u p lift (2 5 6 .7 m a.s.l.), a c c o m p a n ie d b y a s m a ll d e p re s sio n (224.5 m a.s.l.). T h e lack o f w e lls w ith in z o n e s o f o th e r p o ssib le o u tflo w s an d in flo w s fro m a n d to th e b a sin (cf. F ig. 2) does n o t en a b le u s to c o m m e n t on D ż u ły ń s k i’s et al. (1 9 6 6 ) re­

co n stru c tio n o f th e P lio c e n e v a lle y p a tte rn in th e area.

QUATERNARY SEDIMENTS OF TENCZYNEK BASIN

T h e d e sc rip tio n o f Q u a te rn a ry se d im e n ts o f th e T e n c z y ­ n e k B a sin c o n sists o f tw o p arts. T h e first o n e in c lu d e s an a n a ly sis o f w e ll logs w h ię h are th e o n ly so u rc e o f in fo rm a ­ tio n p e rta in in g to th e b a s in s u b s tra tu m . T h e se c o n d p art su m m a riz e s c h a ra c te ristic s o f th e e x p o s e d su rfic ia l d ep o sits.

T h e Q u a te rn a ry b a sin fill c a n b e su b d iv id e d into th ree c o m p le x e s (F ig s. 3 - 5 ) . T h e lo w e r c o m p le x is c o m p o s e d o f g ra v e ls a n d san d s b e a rin g in fre q u e n t in te rc a la tio n s o f d ia m ic to n s. T h e se s e d im e n ts are e ith e r o f flu v ia l (p re-E lste- ria n ) o r g la c io flu v ia l (E ls te ria n ) o rig in . T h e m id d le , g lacio - la c u strin e a n d g la c ia l S an ian (E ls te ria n ) c o m p le x co m p rises c la y s, silts an d d ia m ic to n s, w h e re a s th e u p p e r c o m p lex is

UPPER JURASSIC MIDDLE JURASSIC TRIASSIC

PERMIAN (M E LA P H Y R E ) PERMIAN (DIABASE) CARBONIFEROUS

★ 20

II— II’

BOREHOLES

SAMPLING SITES ^ (PETROGRAPHY) ' CROSS-SECTIONS

Fig. 2. Topography o f the base o f Q uaternary sediments in the Tenczynek Basin

c o m p o se d o f p e rig la c ia l, m o s tly flu v ia l, sa n d s w ith so m e in ­ te rc a la tio n s o f g ra v e ls a n d a n g u la r deb ris.

L O W E R C O M P L E X

T h e lo w e r c o m p le x , up to 19 m th ic k (F ig . 3), m a k e s up the lo w e rm o st p a rt o f th e T e n c z y n e k B a s in fill. Its to p ra re ly e x c e e d s 2 4 5 -2 5 0 m a.s.l. It is c o m p o s e d c h ie fly o f san d s, rarely g rav els, b e a rin g s u b o rd in a te th in la y e rs o f d ia m ic to n s an d clay s. A c c o rd in g to w e ll-lo g d a ta , th e s e g ra v e ls c o m ­ p rise e x c lu s iv e ly lo cal m a te ria l, d o m in a te d b y q u a rtz , lim e ­ sto n es, flin ts, d ia b a s e s a n d in fre q u e n t m e la p h y re s . T h e o n ly on e su rficial e x p o su re o f th is c o m p le x o c c u rs in th e ea ste rn p a rt o f N ie d ź w ie d z ia G ó ra q u a rry (F ig . 4, site 12). In a n a r­

ro w , ste e p -sid e d fu rro w c u t in to P e rm ia n d ia b a s e s (F ig. 2) th ere cro p out silts o v e rla in b y stro n g ly silty an d ru s ty san d s an d san d s w ith g ra v e ls. T h e to p m o s t p a r t o f th e se rie s is c a p p e d b y v a rv e d c la y s, b e lo n g in g to th e m id d le c o m p lex .

P e tro g ra p h ic c o m p o s itio n o f g ra v e ls o f th is c o m p le x (cf.

Fig. 12, sa m p le 14) is re p re s e n te d in th e o u tc ro p b y e x c lu ­ siv ely lo cal m aterial. T h e se a re O x fo rd ia n a n d - ra re ly -

C a llo v ia n lim e sto n e s, C a llo v ia n s a n d s to n e s an d q u a rtz g ra n ­ u le s, b e in g a c c o m p a n ie d b y stro n g ly w e a th e re d clasts o f di­

ab ases.

F ro m th e g e n e tic p o in t o f v ie w , th e lo w e r c o m p le x m ay re p re se n t flu v ia l a n d /o r g la c io flu v ia l se d im e n ts th a t c o u ld h a v e b een d e p o site d b e tw e e n th e late P lio c e n e an d E lsterian ages.

M ID D L E C O M P L E X

T h e m id d le c o m p le x is c o m p o s e d o f c la y s, silts, and d ia m ic to n s, w ith ra re in te rc a la tio n s o f san d s a n d g rav els.

T h e in te rp re ta tio n o f w e lls d rille d in th e stu d y a re a durin g th e last c e n tu ry is re la tiv e ly d iffic u lt, sin ce th e w e ll-lo g ch arts are fa r fro m d e ta il. It is fo r th is re a s o n w h y g lacio - la cu strin e a n d g la c ia l se d im e n ts d rille d b y b o re h o le s are tre a te d h e re to g e th e r; a n o th e r g ro u p is re p re s e n te d b y sands a n d g ra v e ls th a t fo rm in te rla y e rs w ith in th e fo rm e r unit.

T he th ic k n e s s o f se d im e n ts ra n g e s fro m a fe w to ca. 50 m , a v e ra g in g at 4 0 m . T h e ir to p is situ a te d a t 3 1 0 -3 2 0 m a.s.l. in m a rg in a l p a rts o f th e b a sin a n d 2 90 m a.s.l. in its

Complexes Upper

«gss-l Middle I Lower

Fig. 3. Geological cross-sections through Q uaternary infill o f the Tenczynek Basin. D ense hatchure in the m iddle complex unit denotes lenses o f sand and gravel

c en tral, p a rtly e ro d e d p a rt (F ig s. 3, 5).

O u tc ro p s w ith in th e e x c a v a tio n p it a t N ie d ź w ie d z ia G ó ra e n a b le us to id e n tify th e fo llo w in g se d im e n ta ry u n its w ith in the m id d le c o m p le x : v a rv e d c la y s , silts, d ia m ic to n s, as w ell as san d s an d g ra v e ls, th e lith o lo g y o f w h ic h w ill be p re s e n te d b elo w . T h e m o s t e x te n s iv e are silts (F ig . 5);

d ia m ic to n s h a v e sm a lle r e x te n t. V a rv e d c la y s o c c u r at the b a se o f th e c o m p le x , w h e re a s sa n d s a n d g ra v e ls o c c u r s p o ­ ra d ic a lly th ro u g h o u t th e c o m p le x .

Varved clays

V a rv e d c la y s p la y a m in o r ro le w ith in th e m id d le co m -

JURASSIC

PERM IAN (DIABASES) C AR BO N IFERO US LANDSLIDES LOGS STUDIED

CR O SS-SEC TIO N SHOW N IN FIG. 5

Upper com plex M iddle complex Lower com plex 100 m

F ig . 4. Location o f analysed logs o f Q uaternary sediments in the N iedźw iedzia G óra pit

p le x , o c c u rr in g in th e e a s te rn a n d w e s te rn p a rts o f th e e x c a ­ v a tio n p it, a t its b o tto m (F ig s. 6 , 7). T h e ir th ic k n e s s ra n g e s fro m 2 0 c m to 50 cm . T h e v a rv e d c la y s a re c o m p o s e d o f a l­

te r n a tin g lig h t a n d d a rk la m in a e , e a c h p a ir b e in g a fe w m il­

lim e tre s th ic k . L ig h t-g re y la m in a e c o m p ris e silts w ith so m e a d m ix tu re (c a . 10% ; c f F ig. 11, sa m p le l b ) o f cla y , w h e re a s d a rk -g re y la m in a e , 2 m m th ic k , in c lu d e u p to 6 2 % o f clay . T h e C aC C >3 c o n te n t is 5 .0 - 9 .8 % a n d 3 .0 - 6 .5 % , re s p e c ­ tiv e ly .

X -ra y stu d ie s p e rf o rm e d fo r fra c tio n s < 0 .0 0 2 m m , se p a ­ ra te d fro m d a rk la m in a e , in d ic a te p re d o m in a n c e o f fin e ly

d isp e rsiv e sm e c tite w ith a su b o rd in a te a m o u n t o f illite a n d k a o lin ite . Q u a rtz a n d tra c e s o f c a lc ite o c c u r as w ell.

Silts

T h e m a jo r p a rt o f g la c io la c u s trin e s e d im e n ts at N ie ­ d ź w ie d z ia G ó ra is c o m p o s e d o f d a rk -g re y silts, o c c u rrin g p rin c ip a lly in th e c e n tra l p a r t o f th e e x c a v a tio n p it (F ig. 5).

T h e se a re u s u a lly b lu ish a n d b lu is h -g re y , m a s siv e , m o re ra re ly la m in a te d silts th a t c o n ta in in fre q u e n t d ro p s to n e s an d ra re len ses o f g ra v e ls (u p to 1 0 -1 5 % o f g ra v e l fra c tio n ; cf.

F ig s. 10, 11, sa m p le 15). T h e g ra in -s iz e c o m p o s itio n o f g la c io la c u s trin e silts (cf. F ig . 11, s a m p le 6 ) is d o m in a te d by silts w ith a d o z e n o r so p e r c e n t o f sa n d , an d a c o m p a ra b le a m o u n t o f c la y . T h e m e a n g ra in d ia m e te r M z is 5.64—7.09 p h i, i.e. 0 .01- 0 .0 2 m m .

T h e C a C 0 3 c o n te n t w ith in u n w e a th e re d silts ra n g e s fro m 7 .0 % to 13.4% (F ig s. 7, 8). T h e to p m o s t p a rt o f w e a th ­ e re d silts is g re e n ish to y e llo w - g re y a n d c o m p le te ly d e c a lc i­

fied. T h e silts c o n ta in s o m e tim e s th in in te rc a la tio n s o f c la y s, w h o se g ra in -siz e c o m p o s itio n (s a m p le 5: 7 8 % o f cla y ) d oes n o t d iffe r m u c h fro m th a t o f d a rk la m in a e o f v a rv e d c la y s (F ig. 11). X -ra y stu d ie s sh o w p re d o m in a n c e o f sm e c tite , a c ­ c o m p a n ie d b y a d o z e n o r so p e r c e n t o f illite. K a o lin ite , q u artz, as w ell as c a lc ite a n d g o e th ite a d m ix tu re s h a v e also b e e n fo u n d .

P a ly n o lo g ic a l d e te rm in a tio n s re v e a le d a v e ry p o o r a s­

se m b la g e o f p o lle n , c o m p o s e d o f so m e r e d e p o s ite d T e rtia ry ta x a w ith in v a rv e d c la y s a n d in fre q u e n t p o lle n o f Q u a te r­

n a ry c o n ife rs w ith in silts, p o in tin g to a c o ld c lim a te . M i- c ro p a la e o n to lo g ic a l d e te rm in a tio n s , in tu rn , s h o w e d v ery p o o r re d e p o s ite d m ic ro fa u n a , c o m p o s e d m o s tly o f C re ta ­ c e o u s a n d M io c e n e fo ra m in ife rs , In o c e ra m u s p ris m s an d sp o n g e sp ic u le s.

Diamictons

D ia m ic to n s are th e s e c o n d im p o rta n t c o m p o n e n t o f g la-

Q.S.l.

3 2 0

310

300 -

290 -

280 L B E D R O C K SA N D AND

G RA V ELS

V A R V E D C L A Y S

A N GULAR D EBRIS

RECEN T

COLLUV1UM

©

LO G S

1 0 0 m

F ig . 5. Section along the southern exploitation wall o f the N iedźw iedzia G óra quarry. Q uaternary com plexes: LC - lower, MC - middle, UC - upper

cial se d im e n ts e x p o se d a t N ie d ź w ie d z ia G ó ra . T h e y c lu s te r m a in ly in th e e a ste rn p a rt o f th e e x p o s u re (F ig s. 4 , 5, 7, 8) w h e re th e ir th ic k n e ss a tta in s 7 m ; th e y a lso o c c u r in th e c e n ­ tral an d w e ste rn p a rts (F ig s. 4 - 6 ) , a lth o u g h sh o w in g a m u ch sm aller th ick n ess.

T h ese are m o s tly m a s siv e a n d m a trix -s u p p o rte d se d i­

m en ts, so m e tim e s w ith e v id e n c e o f re s e d im e n ta tio n ; clast- su p p o rte d o r in d istin c tly stra tifie d d ia m ic to n s o c c u r s u b o r­

d i n a t e ^ { c f Figs. 6- 8 , and lith o fa c ie s d e sc rip tio n g iv en in th e su b s e q u e n t p a ra g ra p h ).

G ra in -siz e a n a ly s e s (F ig . 11) in d ic a te th a t th e m a in c o m p o n e n t o f d ia m ic to n s a re silts w ith a d m ix tu re s o f san d s, g ra v e ls an d c la y s in v a ria b le p ro p o rtio n s . T h e d ia m ic to n s c o n tain 4 0 - 6 0 % o f g ra in s <0.1 m m , in c lu d in g fro m a fe w to 2 8 % o f c lay s (< 0 .0 0 2 m m ), 5 - 2 0 % o f san d s, a few to 20%

o f g rav els, an d 0 - 9 % o f c la s ts la rg e r th a n 64 m m . T h e larg ­ e st clasts are a few te n s o f ce n tim e tre s in d ia m e te r a n d can be fo u n d o n ly sp o ra d ic a lly a t th e fo o t o f th e e x c a v a tio n w all. T h e ir p e rc e n ta g e w ith in th e d ia m ic to n s is in s ig n ifi­

can t. T h e m e a n g rain d ia m e te r M z is 1 .3 2 -6 .1 6 p h i ( 0 .2 7 - 0.01 m m ), e x c e p tio n a lly a tta in in g 0 .4 4 p h i (0 .7 4 m m ). E x ­ tra p o la tin g th e g ra in -siz e c u m u la tiv e c u rv e b y 2 p h i w ith in sm all fractio n s, o n e c a n o b ta in th e so rtin g in d ex p i o f 3 .4 0 - 6.07 p hi, p o in tin g to v e ry p o o r a n d e x tre m e ly p o o r so rtin g m easu res.

M in eralo g ical stu d ie s p e rfo rm e d on c la y s se p a ra te d fro m d ia m ic to n s (s a m p le s 3 an d 8 ) sh o w a c o m p o s itio n s im ila r to th a t o b s e rv e d w ith in c la y in te rc a la tio n s w ith in silts. T h e C aCC >3 c o n te n t w ith in fra c tio n s < 2 m m c h an g es fro m 7 .5% to 15.8% {cf. F igs. 7, 8 , 10).

S p ecial a tte n tio n h as b e e n p a id to th e p e tro g ra p h ic c o m ­ p o sitio n o f clasts w ith in th e d ia m ic to n s {cf. Fig. 12, sam p les 2, 3, 7, 9, 18). T h e y re p re se n t: lo cal m a te ria l, d e riv e d from the u n d e rly in g su b s tra tu m a n d n e a rb y h ills , m a te ria l d e riv e d fro m th e S o u th a n d C e n tra l P o la n d , as w e ll as ro c k s o f S c a n ­ d in a v ia n a n d th e B a ltic S e a b o tto m p ro v e n a n c e . T h e local m aterial is c o m p o s e d p rin c ip a lly o f w h ite o r w h ite -g re y ish O x fo rd ia n lim e sto n e s, w h o se c la s ts are u su a lly an g u lar, p o in tin g to a v ery sh o rt tra n sp o rt. S o m e o f J u ra ssic lim e ­ sto n es, h o w ev er, c o u ld h a v e b e e n tra n s p o rte d fro m m ore d ista n t a reas situ a te d in th e K ra k ó w U p la n d . T h is ty p e o f m aterial o c c u rs th ro u g h o u t all g ra in -siz e c la sse s, from

< l m m to 2 56 m m , its p ro p o rtio n c h a n g in g d e p e n d in g on g ra in -siz e class a n d sam p le, fro m ca. 1% to > 9 5 % . T h e h ig h e s t a m o u n t o f Ju ra ssic lim e s to n e s h as b e e n e n c o u n te re d w ith in d ia m ic to n s e x p o se d in th e e a s te rn p a rt o f th e p it {cf.

Fig. 12, sa m p le s 3, 7, 9). A n o th e r lo cal c o m p o n e n t is re p re ­ sen ted by c o a rs e -g ra in e d sa n d s to n e s w ith g ra v e ls, d e riv e d fro m th e M id d le Ju ra ssic ro c k s th a t c ro p o u t in th e n o rth e rn p a rt o f th e q u a rry , as w e ll as b y y e llo w is h -b ro w n , lim o n i- tise d sa n d y lim e sto n e s b e a rin g a b u n d a n t fa u n istic re m a in s (C a llo v ia n ). Ju ra ssic lim e s to n e s are a c c o m p a n ie d b y ch e rts an d flin ts. T h e se ro c k s are re la tiv e ly ra re w ith in n e a rb y lim esto n e e x p o su re s, b u t u b iq u ito u s in re g o lith s o f T e rtia ry (P a la e o g e n e a n d P lio c e n e ) a g e (R u tk o w sk i, 1987). S u c h re ­ g o lith s o c c u r in th e stu d y a re a e a st o f N ie d ź w ie d z ia G ó ra {cf. Fig. 12, sam p le 21; see also F ig. 2).

C h e rts are u su a lly d a rk -b ro w n an d g re y , s o m e tim e s y e l­

low . M o re ra re ly , n e a rly b la c k flin ts o f irre g u la r sh ap e, c o v ­ ered by w h ite w e a th e rin g c o a tin g s, ca n b e fo u n d . C h e rts are

Table 1

L ith o fa c ie s c o d e s u se d in lo g d e s c rip tio n (b a s e d on M iall, 1977 a n d E y le s e t al., 1983)

Code Description

Diamictons

Dmm matrix-supported, masive

Dmm(r) m atrix-supported, m assive, w ith evidence o f resedim entation

Dms matrix-supported, stratified diamict;

stratification m ore than 10% o f unit thickness Dmg m atrix-supported, graded, exhibits variable

vertical grading in either matrix or clast content Dmg(s) m atrix-supported, graded, sheared

Dcm clast-supported, masive

Dcm(r) clast-supported, m assive, w ith evidence o f resedim entation

Dcs clast-supported, stratified

Dcs(r) clast-supported, stratified, with evidence o f resedim entation

Gravels

Gp stratified gravel

Sands

Sm massive

Sr rippled

St trough cross stratification

Sh horizontal lam ination

Se erosional scours w ith intraclasts, crude cross bedding

Sd soft-sedim ent deform ation

Silts

Fm massive

FI laminated

Fd w ith dropstones

Fr rootlet traces, seat earth

u s u a lly an g u lar, ra re ly w ell ro u n d e d . T h e ir c o n te n t ch an g es fro m 0 to ca. 10% . S tro n g ly s ilic ifie d ro c k s o f u n c e rta in p ro v e n a n c e , e ith e r P o lish C a rb o n ife ro u s o r S c a n d in a v ia n P a la e o z o ic , can a lso be e n c o u n te re d . T h e d ia m ic to n s c o n ­ ta in a t p la c e s w h ite , lig h t a n d p o ro u s s ilic e o u s m arls (o p o k a s ) o f U p p e r C re ta c e o u s (S e n o n ia n ) age.

A n o th e r im p o rta n t lo c a l c o m p o n e n t a re P e rm ia n d ia b a ­ ses. T h e ir c la s ts w ith in th e d ia m ic to n s im m e d ia te ly o v e rly ­ in g v a rv e d c la y s (F ig. 9; see a ls o F ig. 12, s a m p le 2 ) are u s u ­ a lly an g u lar, stro n g ly w e a th e re d a n d g re y to b ro w n -y e llo ­ w is h . T h e ir c o n te n t w ith in g ra in -s iz e c la s s u p to 128 m m a t­

ta in s ev e n 100% . D ia b a se c la s ts h a v e a ls o b e e n fo u n d in th e d ia m ic to n s e x p o s e d in th e w e s te rn p a rt o f th e p it {cf. Fig. 12, sa m p le 18).

LOG. 1 S W PART

A B C D

Sm Se

Sm

upper complex

Fm

Ft Fd

Dmm (r)

Fi / I Faa complexmiddle

5 5 ^

" v i / ~ ^{1 0} Dms

0 .1

1

11

D m s /D m m Dcs

Cl 12

Dms ^{I R D 13}

Dcs (r)

FI ^{M A X}

8 0 V4

S h

® ' ^1S

- > 1 5 0 K a - 16

silt 5 and

sandintercalations w ith in diamictons

O o a gravel diamic" soil

O ° I . > « tons ) ) ) ) ) ! )

Fig. 6. Sedimentological log o f Q uaternary sediments exposed in the south­

western part o f the quarry (log 1): A - processes and structures, B - lithological log, C - sam pling sites, m axim um clast fraction, palaeotransport directions, D - lithofacies codes; symbols: 1 - depositional contact, 2 - erosional contact, 3 - distinct hiatus, 4 - ripplemarks, 5 - gravity flow, 6 - rootlets, 7 - shear plane, 8 - slip plane, 9 - fault plane, 1 0 - local depression, 11 - deformational horizon with vertical extent o f 0 .1 m, 12 - increase o f C aC 03 content, 1 3 - ice-rafted debris, 14 - maximum clast diam eter in millim etres, 15 - sam pling points, 16 - TL age determinations. For location see Figs. 4 and 5

Q u a rtz g ra in s c o u ld h a v e b e e n d e riv e d e ith e r from S c a n d in a v ia , N o rth e rn P o la n d o r lo c a l ro c k s . In th e last case, th e ir so u rc e are C a llo v ia n sa n d s to n e s (F ig. 4, site 14;

cf. Fig. 12, sa m p le 19), c o n ta in in g 7 0 - 8 5 % o f qu artz, or re- g o lith s o f U p p e r C a rb o n ife ro u s sa n d s to n e s e x p o se d w e st o f T e n c z y n e k (F ig. 12, sa m p le 2 0 ), a n d c o m p ris in g 71—9 6 % o f quartz.

T h e S c a n d in a v ia n m a te ria l is re p re s e n te d firs t o f all b y c ry s ta llin e ro ck s. T h e se are p in k an d g re y g ra n ito id s, ra re ly p in k p o rp h y re s an d g n e is se s. P in k Jo tn ia n q u a rtz ite s o ccu r sp o ra d ic a lly . T h e p ro p o rtio n o f S c a n d in a v ia n ro c k s in indi-

v id u a l s a m p le s c h a n g e s fro m 0 to > 3 5 % . T h ese ro c k s o c c u r in so m e s a m p le s o n ly , b ein g m o st fre q u e n t w ith in d ia m ic to n s e x p o s e d in th e w e s te rn p a rt o f th e p it (cf. Fig. 12, sam p le 18), as w ell as in g la c io flu v ia l g ra v e ls (s a m p le 15).

C ry s ta llin e ro c k s o f S c a n d in a v ia n p ro v e n a n c e a re p re s e n t in all g ra in -siz e classes. T h e la rg e st e rra tic b lo c k s , u s u a lly g ra n ito id s, are in fre ­ q u e n t a n d a tta in a fe w te n s o f c e n tim e tre s in d i­

am eter.

A n im p o rta n t c o m p o n e n t o f th e sed im en ts in q u e stio n are a lso g re y o r b lu e -g re y , so m e ­ tim e s m a rly lim e s to n e s th a t b e a r a b u n d a n t r e ­ m a in s o f b ra c h io p o d s , b iv a lv e s, c rin o id s and, ra re ly , trilo b ite s , d e riv e d fro m O rd o v ic ia n an d S ilu ria n stra ta o f th e s o u th -e a ste rn S c a n d in a ­ v ia. T h e ir o c c u rre n c e is re s tric te d to g lacial d ia m ic to n s w h e re in th e ir c o n te n t a tta in s so m e 25% .

G la c ia l d ia m ic to n s c o n ta in as w ell hard, c o m p a c t lim e s to n e s o f u n k n o w n age. T h ey c o u ld re p re s e n t e ith e r m o re c o m p a c t v a rie tie s o f Ju ra ssic lim e s to n e s o r L o w e r C a rb o n ife ro u s lim e s to n e s th a t cro p o u t n e a r C z a tk o w ic e .

In e x c e p tio n a l c a se s , th e d ia m ic to n s c o n ­ ta in fra g m e n te d sh e lls o f o y ste rs, sev eral m ilim e tre s th ic k , p itte d so m e tim e s b y C lio n a- p ro d u c e d b u rro w s, 1 m m in d ia m e te r. T h e se sh ells h a v e b e e n d e riv e d fro m m a rin e M io cen e strata. T h e re a lso o c c u r fra g m e n ts o f w h ite cal- c iru d ite s a n d m e d iu m - to c o a rs e -g ra in e d c a l­

c a re o u s sa n d s to n e s o f s im ila r p ro v e n a n c e . In a d d itio n , d a rk -g re y , n e a rly b la c k , hard an d c o m p a c t c h u n k s o f lig n ite d e riv e d fro m fre sh ­ w a te r M io c e n e se d im e n ts , h a v e also b e e n fo u n d .

F ro m th e p e tro g ra p h ic p o in t o f v iew , th e d ia m ic to n s o c c u rrin g at N ie d ź w ie d z ia G ó ra c a n be su b d iv id e d in to tw o g ro u p s . T h e first cro p s o u t in th e e a ste rn p a rt o f th e e x p o su re, w h e re th e d ia m ic to n s c o n ta in m a in ly Ju rassic lim e s to n e s (F ig . 12, sa m p le s 3, 7, 9), an d w h o se p e tro g ra p h ic c o m p o s itio n d oes n o t c h a n g e fro m o n e g ra in -s iz e class to an o th er.

T h e o th e r c o m p o n e n ts , lik e c ry s ta llin e ro ck s a n d lim e s to n e s o f S c a n d in a v ia n p ro v e n a n c e , as w e ll as sa n d s to n e s, q u a rtz ite s a n d ch e rts m a k e u p 3 0 % , e x c e p tio n a lly to 4 0 % o f all clasts. J u ­ ra s sic lim e s to n e s are a b u n d a n t b o th in g rav elly a n d m o re c la y e y v a rie tie s o f d ia m ic to n s.

T h e se c o n d g ro u p , o c c u rrin g in th e w e s te rn p a rt o f th e e x p o su re (F ig . 12, sa m p le 18), c o m p rise s m o s tly S c a n d in a ­ v ia n m a te ria l (c ry sta llin e ro c k s a n d L o w e r P a la e o z o ic lim e­

sto n e s), w ith a m in o r a d m ix tu re , u p to few p e rc e n t, o f J u ra s ­ sic lim e sto n e s. T h e re a lso o c c u r c la s ts o f d ia b a se s, w h o se ra tio in c re a se s fro m a few p e r c e n t w ith in sm a ll-siz e g rain s to a d o z e n o r so p e r c e n t in c o a rs e -g ra in e d se d im e n t. Q u artz sh o w s th e o p p o site te n d e n c y .

A n o th e r c h a ra c te r d is p la y tw o s a m p le s o f d iam icto n s c o lle c te d in th e e a ste rn p a rt o f th e p it. T h e m a te ria l im m ed i-

LOG 9 - 1 0 E A S T E R N PART

A B C D E

LOG 8 EAST - CENTRAL PART

D

Dmm(r)/St

Sr

G p FI

FI

Fm

Dms

Dmg

Dmg (s)

D cm (r)

Dcm

Dmm D m m (r)

Dmm

D cm (r) FI

- 7.5 - 7.0 -1 3 .4 -1 3 .2 - 9 7

-15.8

8.3

- 120 135

-1 3 .8

-13.9

—10.6

-10.4 - 5.0 - 65

Fig. 7. Sedimentological log o f Q uaternary m iddle complex sediments exposed in the eastern part o f the quarry (log 9 -10); E - CaC03 content in per cent. For location see Figs. 4 and 5; other explanations in Fig. 6 and Table 1

ate ly o v e rly in g v a rv e d c la y s (F ig s. 7, 12, s a m p le 2 ) c o n ta in s n e a rly e x c lu siv e ly d ia b a s e s, w ith a n e g lig ib le a d m ix tu re (0 .6 % ) o f ch erts an d c ry s ta llin e ro c k s o f S c a n d in a v ia n p ro v e n a n c e . A sa m p le c o lle c te d fro m th e h ig h e r p a rt o f th e sectio n c o n ta in s o n ly a n g u la r fra g m e n ts o f J u ra ssic lim e ­ stones. T h e se se d im e n ts c a n be in te rp re te d as re p re s e n tin g

Fm Sr

FI Fm FI FI Gp FI

12.8

Fd

Fig. 8. Sedimentological log o f Q uaternary middle complex sediments exposed in the east-central part o f the quarry (log 8). For explanations see Figs. 6, 7 and Table 1; location in Figs. 4 and 5

d e b ris flo w s s h e d fro m d ia b a s e o r lim e s to n e w e a th e rin g m a n tle s.

T h e in v e n to ry o f h e a v y m in e ra ls (T a b le 2), fractio n

< 0 .5 m m , is d o m in a te d b y z irc o n . T h e ra tio o f p o o rly re s is­

ta n t (a m p h ib o le s, p y ro x e n e s , a n d a lu s ite , s illim a n ite ) m in e r­

als, m o s t p ro b a b ly g la c ia lly -d e riv e d , is c le a rly h ig h e r in sa m p le 18 th a n in sa m p le 3, w h ic h c o n fo rm s w ith th e h ig h er c o n te n t o f c ry s ta llin e ro c k s in th e fo rm e r sam p le (Fig. 12, sa m p le s 18, 3).

Gravels

T h e m id d le c o m p le x o f g la c ia l se d im e n ts in the T e n c z y n e k B a sin c o n ta in s in fre q u e n t in te rc a la tio n s o f sands a n d g rav els. T h e ir th ic k n e ss, ju d g in g fro m w e ll-lo g d e sc rip ­ tio n , ra n g e s fro m 2 - 3 m to e v e n 10 m (F ig . 3). A n irreg u la r in te rc a la tio n o f g ra v e ls, a d o z e n c m th ic k , has b e e n fo u n d w ith in g la c io la c u s trin e silts (F ig . 10, s a m p le 15) in th e c e n ­ tra l p a rt o f th e pit.

T h e se g ra v e ls (F ig s. 11, 12, s a m p le 15) re p re s e n t a p o o rly so rted m ix tu re o f sa n d , g ra v e l a n d silt. C o b b le s o ccu r sp o ra d ic a lly . P e tro g ra p h ic c o m p o s itio n o f sm a ll-siz e clasts (F ig . 12) is d o m in a te d b y q u a rtz a n d S c a n d in a v ia n -d e riv e d c ry s ta llin e ro ck s, w h o se p ro p o rtio n d im in ish e s w ith th e d i­

m in is h in g grain size. A n o th e r te n d e n c y d is p la y cherts, w h o se ra tio in th e c o a rs e sts fra c tio n s e x c e e d s 5 0 % . Such a fe a tu re is ty p ic a l fo r Q u a te rn a ry g ra v e ls o f th e K ra k ó w re ­ g io n (R u tk o w sk i & S o k o ło w sk i, 1983; R u tk o w sk i, 1995).

128 64 32 16 8 4 2 1 0.5 0 .1 2 6 0.031 0 .0 0 8 0.0 02 m m

128 6 4 3 2 16 8 4 2 1 0.5 0 .1 2 5 0.031 0 .0 0 8 0.0 0 2 m m SANDS AN D

GRAVELS ANG ULAR DEBRIS

TILLS --- SILTS

---VARVED CLAYS F ig. 11. G rain-size com position o f m ain types o f Quaternary sediments in the N iedźw iedzia Góra pit: A - lower complex and varved clays from the base o f the m iddle complex, B - middle complex, C - upper complex

Fig. 10. Sedimentological log o f Q uaternary middle complex sediments exposed in the central-western part o f the quarry (log 3).

For explanatons see Fig. 6 and Table 1; location in Figs. 4 and 5

128 64 32 16 8 4 2 1 0 .5 0 .1 2 5 0.031 0.0 0 8 0.00 2 m m

Fig. 9. Sedimentological log o f Quaternary sediments exposed in the east-central part o f the quarry (log 11 situated above log 9-10). For explanations see Figs. 6 , 7 and Table 1; location in Figs.

4 and 5

LOG 11 EAST C E N T R A L PART

A B C D E

Sm

upper

Sr 0.9 complex

Sh Fr S m Sm Fd ShFm

- 0.0 - 03

m iddle complex

C EN TR A L- W ESTERN PART

8 C D

S h / F I

© S d / G p

S r

S r St S r Sh

LOG 3

O n e sh o u ld ta k e n o tic e o f th e c o m p le te lack o f c a rb o n a te clasts w h ich h a v e p ro b a b ly b e e n d is s o lv e d by g ro u n d w a ­ ters. S im ila r re g u la rity h as b e e n o b s e rv e d th r o u g h o u t g la c ia l sed im e n ts o f th e K ra k ó w , M ie c h ó w a n d W itó w areas (R u tk o w sk i, 1995).

T h e a ss e m b la g e o f h e a v y m in e ra ls d iffe rs fro m th a t o f d ia m ic to n s b y h ig h e r c o n te n t o f z irc o n a n d a sm a lle r a m o u n t o f p o o rly -re s is ta n t m in e ra ls (T a b le 2, s a m p le 15).

T h e g rav els in q u e stio n are o f g la c io flu v ia l orig in . H o w ev er, th e re la tiv e ly h ig h ra tio o f c h e rts in d ic a te s th a t

tra n sp o rtin g w a te r m u s t h a v e b e e n e n ric h e d in e x tra g la c ia l m aterial. T h is is also c o n firm e d b y th e c h a ra c te r o f h ea v y m in e ra l a ss e m b la g e s. T h e la c k o f c a rb o n a te s c a n be a ss o c i­

a te d w ith p o s td e p o s itio n a l d e c a lc ific a tio n .

Discussion

C o m p a rin g th e p e tro g ra p h ic c o m p o s itio n o f d iam icto n s (fra c tio n 1 6 -3 2 m m ) o f T e n c z y n e k B a sin w ith c la y e y tills fro m B ib ic e n e a r K ra k ó w (cf. R u tk o w sk i, 1993) one can c o n c lu d e th a t th e la tte r c o m p ris e 16.4% o f S c a n d in a v ia n

1 0 0-

% 80-

60-

4 0-

Brodła

- 4 - 3 - 2 -1 <

20-

■ł

4 2 mm 64 32 16 8 4 2 mm 16 8 4 2 mm

20

8 0 -

60-

4 0 -

2 0^-

6 - 5 - 4 -3 -2 - V \t V V V '/ V

V V s/ \ V V v \' V V V '/ V

V V s/ \ V V v \' V V V '/ V

V V M \ V V V N> V V V '/ V

V V \J \ V V V \< V V V '/ V

V V Sj \ V V V N' V V v / V

V V \J \ V V V \' V V V '/ V

80-

6 0 -

4 0 -

20-

5 - 4 - 3 - 2 -

V V \/ \ v \' V V

V V y/ \-

V

z

1 _'i

y \

1

80-

60-

40-

20-

—

V, -

X >

O ther rocks Diabases

Igneous and m etam orphic rocks of Scandinavian provenance Flints, cherts

Disintegrated local crystalline rocks

Cretaceous-Tertiary Jurassic

Palaeozoic (Scandinavian) Sandstones, quartzites Quartz

Limestones

Fig. 12. Petrographic com position o f gravel-size fraction. Q uaternary sediments (cf. Figs. 2 and 6 -1 0 ) - upper complex: 17 - debris flow, 16 - gravels; m iddle complex: ! 5 - glaciofluvial gravels, 3 - diam ictons from the eastern part (log 9 -10), 9 and 7 - diam ictons from the east-central part (log 8), 18 - diam icton from the w estern part (log 1), Brodla - diam ictons o f Elsterian age, 2 - debris flow deposits from the base o f log 9-1 0 ; lower complex: 1 4 -g ra v e ls . Pre-Quaternary strata (cf. Fig. 2): 21 - Tertiary (close to N iedźw iedzia Góra), 19 - Callovian (N iedźw iedzia Góra), 20 — U pper Carboniferous regoliths (w est o f Tenczynek)

Table 2

H e a v y m in e ra l c o m p o s itio n (% ) o f Q u a te rn a ry sed im en ts e x p o a se d at th e N ie d ź w ie d z ia G ó ra p it

(det. by M . K ry s o w s k a -Iw a s z k ie w ic z ); fra c tio n < 0 .5 m m

sedim ent diamictons glaciovluvial

gravels coversands

sam ple # 3 18 15 11 13

garnet 36.0 53.5 11.0 25.0 42.0

zircon 26.5 10.5 40.0 38.5 17.5

tourmaline 4.0 3.5 5.5 6.0 5.5

rutile 5.0 2.0 12.0 8.5 1.5

staurolite 2.0 1.5 8.0 4.0 6.5

kyanite 3.5 1.5 1.5 - 1.5

epidote 4.5 4.5 3.5 6.5 11.5

zoisite 0.5 1.0 - 1.0 0.5

titanite 4.5 - 2.5 - -

topase 1.0 2.0 3.5 2.5 1.0

monazite 1.0 2.0 1.5 2.0 1.5

amphibole 6.5 14.5 6.0 3.5 7.0

pyroxene 4.0 2.5 3.5 1.5 2.5

andalusite 1.0 1.0 1.0 0.5 1.0

syllimanite - - - 0.5 0.5

c ry sta llin e ro ck s, 2 0 .7 % o f c h e rts a n d 3 5 .3 % o f u n ­ w e a th e re d Ju ra ssic , S c a n d in a v ia n a n d M io c e n e lim esto n s.

S uch a p ictu re re s e m b le s th a t e n c o u n te re d at N ie d ź w ie d z ia G óra. A s c o m p a re d to g la c io flu v ia l g ra v e ls fro m n o rth -e a s t­

ern P o lan d , th e d e sc rib e d g ra v e ls in c lu d e c o n sid e ra b ly m o re local m aterial at th e e x p e n se o f th e S c a n d in a v ia n one.

T h e d iffe re n c e b e tw e e n c la s ts se p a ra te d fro m d iam ic- to n s a n d th o se o f g la c io flu v ia l g ra v e ls c o n sists in p o std e p o - sitio n al d is so lu tio n o f c a rb o n a te s in th e latter. A n a lo g o u s p ro c e sse s h av e c o m m o n ly b e e n o b s e rv e d w ith in g la c io flu ­ vial se d im e n ts in K ra k ó w (P ro k o c im , L ib ra ry o f C o lle g iu m M ed icu m ) th a t c o m p rise 3 0 .4 % o f c ry s ta llin e ro c k s and

11.7% od ch erts, b u t n o t c a rb o n a te s. A t a n o th e r site w e st o f K rak ó w (B o g u c ia n k a n e a r T y n ie c ), g la c ia l a n d g la c io flu v ia l se d im e n ts c o n ta in 2 6 .4 % o f c ry s ta llin e ro ck s, 19.2% o f ch erts, an d on ly 2 .6 % o f Ju ra s s ic lim e s to n e s d e riv e d from th e b ed ro ck .

U P PE R C O M P L E X

T h e u p p e r c o m p le x is c o m p o s e d p re d o m in a n tly o f san d s w h ic h u n c o n fo rm a b ly o v e rlie th e e ro d e d to p o f se d i­

m e n ts o f th e m id d le c o m p le x . T h e th ic k n e s s o f th is d is c o n ­ tin u o u s c o v e r in th e T e n c z y n e k B a sin d o e s n o t e x c e e d 10 m (Fig: 3, sectio n V I - V I ’). M o re o v e r, th e sa n d s b u ild a v a st c o v e r o v e rly in g o ld e r se d im e n ts u p o n slo p e s a n d in te rflu v e s o f n e a rb y hills, risin g up to 4 0 0 m a.s.l. In fe w cases, th e

san d c o v e r is o v e rto p p e d b y sm a ll d u n e s, p a rtic u la rly w e st o f T e n c z y n e k .

In th e e x c a v a tio n p it a t N ie d ź w ie d z ia G ó ra th e sands are u su a lly y e llo w -g re y is h , ra re ly ru s ty , a n d m e d iu m to fin e ­ g ra in e d (Fig. 11, sa m p le s 11, 13). T h e y are e ith e r rip p le d , m assiv e o r sh o w in g h o riz o n ta l la m in a tio n . In fre q u e n t e ro sio n a l sc o u rs are to be e n c o u n te re d as w ell. T he m ean grain d ia m e te r M z is 1 .6 9 -1 .8 8 p h i (0 .2 7 -0 .3 1 m m ). T he sands are m o d e ra te ly s o rte d ( c i 0 .6 4 -0 .6 9 ) . C o a rse -g ra in e d sa n d g ra in s re v e a l su rfa c e s in d ic a tiv e o f a e o lia n rew o rk in g . T h e san d s are m o s tly d e v o id o f c a rb o n a te s o r c o n ta in a m i­

n o r a d m ix tu re o f CaCC>3.

T h e v a ria b le p ro p o rtio n o f re s is ta n t a n d n o n re s ista n t h ea v y m in e ra ls (T a b le 2 ) in d ic a te s th a t th e s e san d s h a v e b e e n d e riv e d b o th fro m g la c ia l s e d im e n ts a n d p re -Q u a te r- n a ry b ed ro ck .

T he b a se o f th e s a n d c o v e r (F ig s. 5, 6 , 9) co n ta in s at p la c e s a m a rk e d a d m ix tu re o f g ra v e ls. T h e m e a n g rain d i­

a m eter M z is is h e re 0 .2 7 p h i (0.83 m m ), th e so rtin g is very p o o r ( a i ca. 3.2 p h i), a n d g rav els are u su a lly c o m p o sed o f d iab ase c la s ts (F igs. 5, 12, s a m p le 16). S o m e o f th e s e clasts are u n w e a th e re d o r sh o w tra c e s o f a e o lia n rew o rk in g .

In th e e a ste rn p a rt o f th e p it (F ig s. 4, 5, lo g 13, Fig. 12, sam p le 17) an in te rla y e r o f a n g u la r d eb ris, 0.5 m th ick , has b een fo u n d w ith in th e san d s. It c o m p rise s 5 2 .7 % o f gravel a n d 5 .9% o f c o b b le -siz e fractio n . T h e m ean g rain d iam eter M z is 2 .0 7 p h i (0 .2 4 m m ), th e s o rtin g is v ery p o o r ( o i 3.23 p hi), an d th e la rg e st clasts a tta in a d o z e n c e n tim e tre s in d i­

a m e te r (Fig. 11). T h e la tte r are m a in ly a n g u la r frag m en s o f O x fo rd ian lim e sto n e s w ith su b o rd in a te a d m ix tu re o f san d y a n d o rg a n o g e n ic C a llo v ia n lim e s to n e s (Fig. 12, sa m p le 17).

T h e w h o le in te rc a la tio n a p p e a rs to re p re s e n t a so liflu ctio n to n g u e.

DIAMICTON LITHOFACIES OF THE MIDDLE COMPLEX: DESCRIPTION

T he m id d le c o m p le x c o m p ris e s th e m a jo r p a rt o f se d i­

m en ts e x p o se d at th e N ie d ź w ie d z ia G ó ra p it (Fig. 5) and, th e re fo re , p ro v id e s so m e c lu e s to s e d im e to lo g ic a l in te rp re ­ ta tio n o f g la c ig e n ic s e d im e n ts o f th e E lste ria n stage. T he p o o r state o f e x p o su re d o e s n o t a llo w u s to d raw a d etail p ic ­ tu re o f sp atial d is trib u tio n o f in d iv id u a l d ia m ic to n lith o fa- cies; th e fo llo w in g d e s c rip tio n is b a s e d on a fe w logs w h ich w ere a c c e ss ib le to o b se rv a tio n (F ig s. 4 - 1 0 , T a b le 1).

Matrix-supported, massive diamictons [Dmm]

T h e se d e p o sits o c c u r in lo g s 9 - 1 0 a n d 1 (F ig s. 6 , 7), b e ­ ing re p re se n te d b y 0.4 to 1.1 m th ic k b o d ie s o f b ro w n an d b ro w n -g re y d ia m ic to n s w ith in fre q u e n t, c h a o tic a lly d is ­ p e rs e d clasts 0 .5 -1 c m to 7 c m in d ia m e te r, a v e ra g in g a t 2 - 4 cm . N o stria tio n o r p o lis h in g h as b e e n fo u n d . T h e C a C 0 3 c o n te n t in c re a se s fro m th e b o tto m u p w a rd s.

Matrix-supported, massive diamictons with evidence o f resedimentation [Dmm(r)]

T h ey b u ild le n tic u la r b o d ie s , 1 0 -4 5 c m th ic k , o b serv ed at logs 9 - 1 0 , 8 an d 1 (F ig s. 7, 8 , 6 ) a n d c o m p o s e d o f dark - b ro w n , c a lc a re o u s, c la y e y d ia m ic to n s, re s tin g w ith in m a s­

sive, b ro w n -g re y a n d c a lc a re o u s s e d im e n ts w ith sm a ll clasts o f lim esto n es (lo g 9 - 1 0 ) . A t th e to p o f log 9 - 1 0 (F ig. 7) th e se d ep o sits are re p re s e n te d b y w e d g e s o f c la y e y d ia m ic - to n s, u n d e rla in b y a 2 0 - 3 0 c m th ic k la y e r o f la c u strin e rh y th m ite s, e m b e d d e d w ith in v e ry fin e -g ra in e d a n d silty sands. T h e w h o le u n it is h e re s tro n g ly d is tu rb e d a n d c u t on th e S W by a n o rm a l fau lt, se p a ra tin g th e d ia m ic to n s fro m la cu strin e silts. T h e d ia m ic to n s o f lo g 8 (F ig . 8) b e a r rare clasts, 0 .5 -3 cm in d ia m e te r, a n d is o la te d le n s e s o f light- g rey silts an d e llip s o id a l lu m p s o f v e ry fin e -g ra in e d and silty san d s, 6 15 c m in size. T h e y are u n d e rla in b y m a ssiv e silts w ith ic e -ra fte d d eb ris a n d o v e rla in b y la m in a te d silts. It is the o n ly o n e in te rla y e r o f d ia m ic to n s o b s e rv e d in th is log.

In log 1 (Fig. 6), 20 c m -th ic k le n s e s o f m a s s iv e d ia m ic to n s w ith lu m p s o f san d s e m b e d d e d w ith in silt-c la y e y m a trix , and b e a rin g in fre q u e n t cla sts 2 - 5 m m to 1 cm in d ia m e te r, h av e b een found.

Matrix-supported, stratified diamictons [Dins/

T h e to p m o st p a rt o f d ia m ic to n se rie s in lo g 9 - 1 0 (Fig.

7) is re p re se n te d b y 1.3 m th ic k b ro w n -g re y , s tro n g ly c a l­

c a re o u s, d ia m ic to n s w ith irre g u la r in te rc a la tio n s o f silts an d sh o w in g fa in t la m in a tio n . C la sts are sm a ll an d in fre q u e n t, u su ally 2 - 4 m m to 2 cm in d ia m e te r, a n d c h a o tic a lly o rie n ­ tated . In th e to p m o s t p a rt, is o la te d c la s ts o f Ju ra ssic lim e ­ sto n es, 5 - 7 cm acro ss, o c c u r. In lo g 1 (F ig . 6 ), th is lith o fa- cies o ccu rs tw ic e . T h e lo w e r la y e r is 0 .8 m th ic k a n d c o m ­ p o se d o f grey d ia m ic to n s w ith is o la te d c la s ts 0 .5 -1 c m to 3—

5 cm in d iam eter, in c lu d in g le n tic u la r b o d ie s o f fin e ly lam i­

n a te d silts, 5 - 8 cm long. T h e u p p e r p a rt o f th is la y e r b ears m o re len ses o f c ro s s-la m in a te d , w h ite -g re y silts, a lte rn a tin g w ith silty clay s a n d ste e l-g re y c la y s. L e n tic u la r s ilt b o d ie s, 2 - 4 cm th ic k a n d 5 - 6 cm lo n g , re s e m b le flo w stru ctu res.

T he to p m o st p art, 2 0 cm th ic k , sh o w s d is c o n tin u o u s w a v y lam in atio n . T he se c o n d , u p p e r la y e r o f D m s in lo g 1 (F ig . 6) is 1.5 m th ic k an d c o m p o s e d o f g re y d ia m ic to n s w ith c h a o ti­

cally o rie n ta te d clasts, 0 .5 - 2 cm in d ia m e te r, a n d b e a rin g thin, irreg u la r len ses e n ric h e d in c la s ts 2 - 3 m m to 1.5 cm in d iam eter.

Matrix-supported, graded diamictons [Dm g]

T h e se are 0.5 m th ic k b o d ie s o f g re y -b ro w n , c a lc a re o u s d ia m ic to n s o c c u rrin g in lo g 9 - 1 0 (F ig . 7). T h e y c o n ta in clasts 2 - 3 m m to 1 -2 .5 c m in d ia m e te r, th e ir size d e c re a s in g fro m th e b o tto m u p w a rd s. T h e to p is tr u n c a te d b y a m e lt-o u t d ep re ssio n , 1 m in d ia m e te r a n d 0 .5 - 0 .6 m d e e p , fille d w ith g re y -b lu ish silts.

Matrix-supported, graded and sheared diamictons [Dmg(s)l

In log 9 - 1 0 (F ig. 7) th e y are re p re s e n te d b y a 1.4 m th ic k la y e r o f g re y -b ro w n , c a lc a re o u s d ia m ic to n s w ith clasts 0 .5 -1 c m to 6 - 7 cm in d ia m e te r, a v e ra g in g at 2 - 3 cm . T he d ia m ic to n s are m a ssiv e , sh o w p la ty fis s ility , a n d a re c u t at p la c e s b y su b v e rtic a l jo in ts . A p a rt fro m d o m in a n t Ju ra ssic lim esto n es, c h e rts 3 - 3 .5 c m in d ia m e te r an d in fre q u e n t q u a rtz g ra n u le s, 1 cm acro ss, are to b e fo u n d . T h e c o n ta c t w ith u n d e rly in g D c m (r) is sh e a re d , th e u p p e r b o u n d a ry o f s e d im e n ta ry ch a ra c te r.

Clast-supported, massive diamictons [Dcm ]

In log 9 - 1 0 (F ig. 7) th e s e a re 2.1 m th ic k lig h t-g re y an d b ro w n -g re y , m a s siv e d ia m ic to n s w ith n u m e ro u s clasts, 2 0 - 2 7 cm to 60 c m in d ia m e te r, d o m in a te d b y J u ra ssic lim e ­ sto n es. T h e b a se is o f te c to n ic c h a ra c te r; th e w h o le u n it is tilte d to S 2 0 °W . T h in in te rla y e rs o f lig h t-g re y d ia m ic to n s o c c u r as w e ll. T h e C aC C >3 c o n te n t is v a ria b le , fro m m o d e r­

ate to sig n ific a n t. T h e to p is tr u n c a te d b y a d e p re s sio n , 4 .5 -5 m lo n g an d 0.6 m d e e p , p ro b a b ly o f m e lt-o u t o rig in , filled w ith a 5 cm th ic k la y e r o f la m in a te d c la y s o v e rla in b y bluish m a s siv e silts.

Clast-supported, massive diamictons with evidence o f resedimentation [Dcm (r)]

In log 9 - 1 0 (F ig . 7), th e s e d e p o s its im m e d ia te ly o v erlie th e b asal v a rv e d c la y s a n d fo rm a n in te rc a la tio n w ith in the m id d le p a rt o f th e d ia m ic to n se rie s. T h e lo w e r la y e r is re p ­ re s e n te d b y y e llo w -b ro w n a n d ru s ty , sa n d y , c a rb o n a te -fre e lo a m s, b e a rin g a b u n d a n t a n g u la r d e b ris o f d ia b a s e s, 0 .5 -7 .0 c m in d ia m e te r, a v e ra g in g a t 1 .2 -2 .5 cm . N o tra c e s o f S can ­ d in a v ia n m a te ria l h as b e e n fo u n d . T h e la y e r d ip s 2 0 0 /2 0 and re s e m b le s a d e b ris-flo w d e p o s it s h e d fro m th e n e a rb y slope.

T h e u p p e r la y e r in th is log, a lso o f th e d e b ris -flo w ty p e, is re p re se n te d b y g re y lo a m s w ith a b u n d a n t a n g u la r d eb ris o f Ju ra ssic lim e s to n e s, 2 - 3 c m in d ia m e te r.

Clast-supported, stratified diamictons [D csj

In log 1 (F ig . 6) th e s e d e p o sits, 2 0 c m th ic k , re s t w ith in D m s se d im e n ts. T h e se are s a n d y d ia m ic to n s w ith n u m e ro u s c la s ts 2 - 5 m m to 2 - 3 cm in d ia m e te r.

Clast-supported, stratified diamictons with evidence o f re- sedimentation [Dcs(r)]

In log 1 (F ig. 6 ) th e y im m e d ia te ly o v e rlie th e basal v a rv e d clay s. T h e se are 20 c m th ic k , ru s ty -b ro w n , san d y silts b e a rin g a n g u la r c la s ts o f d ia b a s e s, 0 .5 - 8 cm in d ia m e ­ ter, as w ell as e rra tic c la s ts, 5 c m a c ro s s. T h e b a se is ero- sio n al, th e c o n ta c t w ith o v e rly in g d e p o s its b e in g o f s e d i­

m e n ta ry c h a ra c te r.

Discussion

T he th ic k e s t series o f d ia m ic to n s h a s b e e n fo u n d in the e a ste rn an d e a s t-c e n tra l p a rt o f th e N ie d ź w ie d z ia G ó ra pit.

T h e ce n tra l a n d w e ste rn p a rts b e a r n o o r o n ly iso la te d , thin, le n se -lik e b o d ie s o f d ia m ic to n s (F ig. 5). T h e se b o d ie s eith er o v e rlie th e b a sa l v a rv e d c la y s (lo g s 1 a n d 9 - 1 0 ; F ig s. 6 , 7) or fo rm irre g u la r in te rc a la tio n s w ith in m a s siv e o r - ra re ly - la m in a te d silts w ith d ro p s to n e s. P o o r sta te o f th e e x p o su re d o es n o t allo w fo r re c o n s tru c tio n o f th e d ia m ic to n a rc h ite c ­ tu re; it ap p ers, h o w e v e r, th a t in d iv id u a l la y e rs are d is c o n ­ tin u o u s an d c e rta in ly do n o t re s e m b le lo d g e m e n t tills. T he p re d o m in a n tly m a trix -s u p p o rte d d ia m ic to n s, e ith e r sh o w in g tra c e s o f re s e d im e n ta tio n o r c ru d e s tra tific a tio n , u n d e rlin e d b y th in in te rla y e rs o f silts o r sa n d s, p ro b a b ly re p re s e n t flow tills o r - at le a st in c ase o f so m e o f th e la y e rs in lo g 9 - 1 0 (F ig. 7) - m e lt-o u t tills (cf. c rite ria liste d in B e n n e tt & G las- ser, 1996). T h e c la s t-s u p p o rte d d ia m ic to n v a rie tie s, fo u n d b o th in lo g 9 - 1 0 (F ig. 7) a n d 1 (F ig. 6 ) re p re s e n t d e b ris flow d ep o sits, p ro b a b ly s h e d fro m n e a rb y slo p e s b u ilt u p from P e rm ia n d ia b a s e s o r J u ra s s ic lim e s to n e s.