Fragments of exotic rocks in the pelagic deposits of the Bathonian of the Niedzica Series (Pieniny Klippen-Belt, Carpathians)

R O C Z N I K P O L S K I E G O T O W A R Z Y S T W A G E O L O G I C Z N E G O A N N A L E S D E L A S O C l E T E G £ O L O G I Q U E D E P O L O G N E

T o m (V o lu m e ) X X X — 1960 Z e s z y t ( F a s c i c u le ) 1 K r a k ó w 19i0

KRZYSZTOF BIRKENMAJER, STANISŁAW M. GĄSIOROWSKI I TADEUSZ WIESER

EGZOTYKI W OSADACH PELAGICZNYCH BATONU SERII NIEDZICKIEJ PASA SKAŁKOWEGO POLSKI

(Tabl. V III—X i 5 fig.)

Fragments of Exotic Rocks in the Pelagic Deposits of the Bathonian of the Niedzica Series

(Pieniny Klippen-Belt, Carpathians)

(PI. V III—X and 5 fig.)

STRESZCZENIE

W batońskiej części w apienia bulastego dolnego serii niedzickiej w Czajakowej Skale na południe od Jaw orek koło Szczawnicy znalezio­

no 32 egzotyczne fragm enty skał magmowych (porfiry kwarcowe m ikro- granitowe, mikropegmatytowe, granofirowe i felzytowe — wszystkie komagmatyczne, tu f porfirowy i aplit), m etam orficznych (granitognejsy dwumikowe i biotytowe, gnejsy muskowitowe, gnejsy oczkowe biotytowe) i osadowych (wapień). Fragm enty te są nieregularnie rozrzucone na eliptycznej powierzchni około 2 m 2, równoległej do warstwowania. Po obróceniu do położenia poziomego dłuższa oś tej elipsy przebiega NW-SE.

Niektóre fragm enty tkw ią w skale ukośnie w stosunku do powierzchni warstwowania, inne zaś równolegle. Duże fragm enty zagłębiły się w osa­

dzie nieco bardziej niż małe. Te ostatnie prawdopodobnie w skazują po­

w ierzchnię dna w chwili depozycji fragmentów. Stosunek fragm entów skał egzotycznych do konkrecji wapienia bulastego jest przypadkowy.

W ydaje się więc, że w apień bulasty był częściowo zdiagenezowany w chwili ich depozycji. Wielkość fragm entów w aha się od 0,5 cm do 45,0 cm, ciężar wszystkich fragm entów wynosi 65,7 kg.

Dla poszczególnych fragm entów zostały określone: współczynniki / b c \

Z i n g g a i |} kulistość (według „praktycznego w zoru” W a d d e - 1 a), stopień obtoczenia (według skali P e t t i j o h n a ) i współczynnik

I a -)- b ^ ^

A. C a i l l e u x I 2c r Z analizy tych wartości w ydaje się, że kształt

fragm entów jest bardziej zbliżony do kształtu otoczaków rzecznych niż plażowych morskich.

Wapień bulasty dolny serii niedzickiej był niewątpliwie osadem pe~

lagicznym i batialnym lub naw et abyssalnym. W ydaje się, że najp raw ­ dopodobniej szym sposobem transportu fragm entów egzotycznych skał znalezionych w Czajakowej Skale z lądu w strefę sedym entacji w apienia bulastego dolnego był transport w korzeniach dryfującego drzewa lub przez „wyspę pływ ającą”, w yrw aną przez powódź i zniesioną przez rzekę do morza. W każdym razie trzeba wykluczyć w yrzucenie frag­

m entów przez w ybuch wulkanu, transport przez prąd zawiesinowy, przez górę lodową, przez zwierzęta (jako gastrolity) i przez glony w yrw ane z dna.

Małe fragm enty egzotyczne w ystępują sporadycznie i pojedynczo także w innych wapieniach bulastych, w radiolarytach i w biancone pienińskiego pasa skałkowego. Skały zawierające je są również pelagicz- ne i batialne lub abyssalne. Fragm enty egzotyczne mogły zatem być przetransportowane przez dryfujące drzewa lub przez „wyspy pływ a­

jące” albo też przez glony w yrw ane z dna.

Jeżeli się założy, że wszystkie fragm enty egzotyczne znalezione w Czajakowej Skale pochodziły z tego samego lądu, to można się starać zrekonstruować z nich najprostszą możliwą budowę geologiczną. Byłaby ona następująca: m asyw krystaliczny (granitognejsy i gnejsy) intrudo- wany w dolnej części aplitami, w górnej porfiram i, przykryty produk­

tami wybuchów kwaśnych wulkanów (porfiry felzytowe i tu f porfiro­

wy) i skałami osadowymi (wapień prawdopodobnie triasowy). Jeżeli się założy, że ląd, o którym mowa, znajdował się w geosynklinie karpackiej (na co istnieje wiele danych dyskutowanych w pracy), można by przez analogię ze znanym i profilam i stratygraficznym i starszego kompleksu skalnego K arpat określić wiek m asywu krystalicznego jako przedgórno- karboński, intruzji i ekstruzji — jako górny karbon-perm , tej zaś części osłony osadowej, którą reprezentuje w apień — jako środkowy trias.

Z masywów krystalicznych w geosynklinie karpackiej nie mogły do­

starczyć egzotyków do Czajakowej Skały: krystalinikum tatrzańskie i masyw egzotykowy między basenam i pienińskiego pasa skałkowego a serii wierchowej sensu lato (ze względu na charakter petrograficzny skał magmowych), m asyw między basenami serii niedzickiej i braniskiej (ponieważ nie był w batonie wynurzony). Natomiast mogły dostarczyć tych egzotyków m asywy krystaliczne K arpat zewnętrznych. Skład p etro g ra­

ficzny najbardziej południowego z nich, to znaczy m asywu między ba­

senem serii czorsztyńskiej a bruzdą czetechowicką i jej wschodnim prze­

dłużeniem, jest uderzająco podobny do składu opisanych w tej pracy egzotyków. Ponadto masyw ten był w batonie najbliższym basenu serii niedzickiej lądem.

— 30 —

Pracownia Geologiczno-Stratygraficzna Polskiej A ka d em ii N a u k w Krakowie

i

In stytu t Geologiczny w Warszawie

— 31 —

A b s t r a c t . Some exotic fragm ents of igneous, m etam orphic an d sedim entary rocks occur in th e B athonian of the Niedzica Series, Pieniny K lippen-B elt of Poland. The shape of th e fragm ents suggests alluvial gravel. The fraigments a re enclosed in th e pelagic and b ath y al n odular lim estone. T heir deposition w as u n d o u b ­

tedly sim ultaneous w ith th a t of the enclosing rock. The m ode of tran sp o rta tio n of these exotic fragm ents is discussed, and it is suggested th a t tran sp o rtatio n by driftw ood or by a „floating island” of tangled grow th is the m ost probable.

An attem p t is m ade to reconstruct the stratig rap h ic sequence in the lan d th e exotic fragm ents derived from, and to determ ine the position of this land in the C arpathian geosyncline.

A. GEOLOGICAL PART

by K. B irk en m ajer and S. M. G^siorowski

The Niedzica Series has been formed along the northern border of the central p art of the Pieniny K lippen-B elt sedim entary basin. The prim itive position of the Niedzica Series was between the sedim entary regions of the Czorsztyn Series to the north and of the Branisko Series to the south ( B i r k e n m a j e r , 1953, 1957a, B i r k e n m a j e r - Z n o - s k o, 1955).

N otwithstanding the m any features common w ith the other Klippen Series, the individuality of the Niedzica Series is quite clear. As to the

Fig. 1. A. The position of the Pien'iny K lippen Belt in the C arpathians. A rectangle m ark s the region indicated in Fig. 1 B; C — Czorsztyn, NT — Nowy Targ, Z —

Zakopane

B. O utcrops of the Niedzica Series in th e K lippen Belt of Poland (after B irkenm ajer, 1959 a, simplified). The klippes of the Niedzica Series in black.

CS — Czajakow a Skała

— 32 —

not individual features, from the Aalenian to the Callovian the Niedzica Series has more in common w ith the Czorsztyn Series th an w ith th e Branisko Series, and from the Callovian upw ards the relation is rev er­

sed.

In the Subhercynian movements the Niedzica Series has been torn up and dragged as blocks and lenses below the Branisko Nappe n o rth ­ wards over the Czorsztyn Series, then autochthonous ( B i r k e n m a j e r ,

1958a). Subsequent tectonic movements deformed the Niedzica Series still more. The very great tectonic deform ation makes difficult the inve­

stigations of the stratigraphy of the Niedzica Series.

The Niedzica Series in the Polish p art of Spisz and near Szczawnica occurs now as small klippes separated by rocks belonging to other series. East of Szczawnica, in the environs of Jaw orki and Biała Woda, however, the klippes of the Niedzica Series are greater ( B i r k e n m a ­ j e r , 1959a) (Fig. 1), and outcrops are better. It is in this region that the exotic fragm ents have been found.

GEOLOGICAL POSITION OF THE EXOTIC FRAGMENTS

L o c a l i z a t i o n o f t h e E x o t i c F r a g m e n t s

Czajakowa Skala is a klippe situated on the right side of the gorge Horn ole near Jaw orki east of Szczawnica. It has been described for the first tim e by V. U h l i g (1890, Fig. 31, 33), who considered it to be formed by the Subpieniny (Czorsztyn) Series rocks. The same view was held by L. H o r w i t z and F. R a b o w s k i (1929), though on a pro­

file included in their paper (op. cit., Fig. 7) radiolarites w ere m arked.

K. B i r k e n m a j e r (1953) considers Czajakowa S k a la¹ to be formed by the Niedzica Series rocks. This view is adopted in the present paper.

A detailed description of the stratigraphical sequence in the Czajakowa Skala is given iby B i r k e n m a j e r (1958a, Excursion No 20); see Fig. 2.

In the SE. part of the klippe Czajakowa Skala there is a nearly vertical dip-slope about 15 m etres high, form ed by th e Lower N odular Limestone. This limestone can be subdivided into:

c. dark red nodular limestone ^{1 . 2} m. thick b. dark red thin bedded haem atite m arl 0.5 m. thick a. dark red nodular limestone ^{6 . 0} m. thick

total thickness 7.7 m.

The exotic fragm ents occur in the lower part (a), c. 1.3 m. from the sedim entary contact of the Lower Nodular Limestone w ith the Red Crinoidal Limestone, and c. 7 m. above the scree at the foot of the dip-slope. Their occurrence is lim ited to an elliptical surface c. ² square metres, parallel to the stratification. The longer axis of the surface when turned to a horizontal position runs NW-SE. There are 32 exotic frag­

ments. They are scattered in a haphazard w ay w ith the exception of

1 Described (op. cit.) urfder the nam e „U pper Homola G orge”.

— 33 ■—

a not too distinct increase of concentration of greater fragm ents tow ards SE. (fig. 3A.). Some fragm ents m ust have lain on the bottom on th eir flat sides; the sm aller ones presum ably indicate the position of the bottom

Fig. 2. Profile of Czajakowa Skała near -Jaworki (after B irkenm ajer, 1958a, fig. 116, modified). The Czorsztyn Series: 1. N odular Lim estone (Callovian to K imeridgian).

The Niedzica Series: 2. Red Crinoidal Limestoa'e (Bajocian), 3. Low er N odular L im estone (Bathonian-Callovian), — th e position of exotic fragm ents is m arked by a thick d o t indicated by th e le tte r E, 4. Low er Red R adiolarites, G reen R adiolarites, U pper Red R adiolarites (Oxfordian), 5. U pper N odular Lim estone (Kimeridgian), 6. Calpionella Lim estone (Tithonian), 7. Pseudocherty Lim estone (V alanginian-H auterivian), 8. Beds w ith globiigerinids and radiolarians (B arrem ian-

-Albian). Scree m ark ed w ith dots

on which they have been deposited, while the greater ones have sunk a little in the sediment. O ther fragm ents are enclosed in the sedim ent

obliquely or perpendicularly to the stratification (Fig. 3B).

The enclosing nodular limestone consists of distinct limestone nodules separated by a m arly substance. Some nodules are deformed internal moulds of shells of ammonites and nautiloids up to a few score cen­

tim etres in diameter. The nodular limestone is strongly coalesced w ith th e exotic fragments. The nodules imm ediately above (in the stratigra- phic sense) the greater exotic fragm ents are somewhat flatter than the usual nodules. Nodules below the greater exotic fragm ents have been completely destroyed by erosion. It seems th a t the fragm ents did

3 R o c z n i k P T G

— 34 —

not form the nuclei of the nodules, nor did the m arly substance tend to accumulate on th eir surfaces. Their relation to the particular nodules seems quite haphazard.

7 15 2V 24

f t - — — — a

•>0 j q ??

Fig. 3. A. Position of th e exotic fragm ents in the Low er N odular Lim estone on .bottom of the layer

B. a-a, b-b, c-<c, d-d — tran sv ersal sections of the layer w ith the exotic fragm ents (cf. Fig. 3A)

The small am ount of sinking into the bottom seems to indicate th at the sedim ent has not been very soft w hen they fell down. It seems, therefore, th a t the nodules w ere already formed, and the sedim ent partly diagenezed, w hen the exotic fragm ents fell down.

In some of the exotic fragm ents jointing is visible. It does not pass into the enclosing rock. Some joint cracks are filled w ith calcite, others are empty. These phenom ena could result owing to difference in com­

petence of the exotic fragm ents and of the enclosing rock.

— 35 —

P e t r o g r a p h i c C h a r a c t e r a n d S h a p e A n a l y s i s o f t h e E x o t i c F r a g m e n t s

The Table given below (Table 1) contains the complete list of exotic fragm ents in question. P articular fragm ents are designated by the same num bers as in Figure 3A. The petrographic character of igneous and m etam orphic rocks has been determ ined by T. W i e s e r. Diam etres a, b, c, are at right angles, bu t do not always cross one another.

It has been assumed th a t all the exotic fragm ents are of an appro­

xim ately ellipsoidal shape. The approxim ate w eight has been obtained by m ultiplying th e volume of a fragm ent obtained on the above assum p­

tion by 2.7 (mean specific w eight of Sial after Umbgrove, 1947).

Z i n g g ’s (1935) diagram has been used (Fig. 4) to compare the rela-

c b

tions ~ and ~ of the particular fragments. As the qu an tity of the exotic fragm ents was small, we did not take into account the size and the petrographic character.

a + b

The relation 2c , w hich according to A. C a i l l e u x (1945) clearly depends on the rounding agent, was determ ined for the particular frag­

m ents (cf. Table 1).

■« **-- 1

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Fig. 4. Relations - - and — in Zingg’s diagram

a b

Sphericity has been determ ined according to W a d e 1 l’s „practical form ula” ip = — , where ip is sphericity, d„ — the diam eter of a sphere

S

of the same volume as the fragm ent, Ds — the longest diam eter of the fragm ent (cf. K r u m b e i n , 1938, pp. 292—294). The results are presented in Table 1.

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— 36 —

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Roundness has been determ ined according to P e t t i j o h n ’s (1949, pp. 51—53) scale (Table 1 and 2).

T a b l e 2 Roundness of the exotic fragments

Roundness Frequency- Percentage

Angular ^_

Subangular 15 46,9

Subrounded 6 18,7

Rounded 11 34,3

Well rounded — —

32 99,9

The results of the shape analysis of our exotic fragm ents do not allow more than tentative conclusions. The quantity of our fragm ents is sm aller th an th a t generally used in sedimentological study, and the size and the petrographic character could not be taken into account to such an extent as th ey generally are. This som ewhat invalidates com­

parisons. Besides, the quantity of our fragm ents is very small. In the last place, it m ust be assumed th a t all our fragm ents derived from the same environm ent. Nevertheless, th e results of the shape analysis perm it us to advance certain suggestions as to the sediments our frag­

ments derived - from.

c b

The relations and ~ of our fragm ents which are m ostly (74.9 per cent of quantity — cf. Table 3) porphyry do not differ m uch from the same relations obtained for the granite pebbles 64— 128 mm. long in the upper course of the river Dunajec (after 59 km. of transport — cf. U n r u g , 1957, Fig. 12A). According to A. C a i l l e u t x (1945, p. 394)

a + b

the relation —~ for the porphyry river fragm ents oscillates w ith great variations about 1.8, and for the porphyry beach fragm ents about 2.4.

a + b

For our porphyry fragments, the m ean arithm etic relation ~ is 2.0 (Table 3). The degree of roundness of our fragments, which is not high, is another difference from the beach fragments, which are usually very well rounded.

It seems, therefore, th at the shape of our fragm ents resembles rath er the shape of the alluvial fragm ents th an th a t of the beach fragments.

This means th a t our fragm ents derived rath e r from alluvial deposits than from beach deposits, as, according to C a i 11 e u *x (op. cit., p. 400):

„Ainsi se trouve ecartee une im portante cause d ’erreu r dans l’etude des formations anciennes: au voisinage d’une embouchure, le m ateriel fluviatile, repris par la mer, perd tres vite son caractere fluviatile”.

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S e d i m e n t a r y C o n d i t i o n s o f t h e L o w e r N o d u l a r L i m e s t o n e

The terrigenic adm ixture in the Lower Nodular Limestone consists almost exclusively of clay (sensu P e t t i j o h n , op. cit., pp. 12— 13).

The only fragm ents greater than clay hitherto found are the above described exotic fragments.

The continuous and very slow sedimentation, the apparent unifor­

m ity in the horizontal sense, the sedim entary contact w ith the radio- larites, and the lack of terrigenic m aterial greater th an clay, taken together, imply a sedim entation in pelagic and bathyal, if not abyssal,

conditions.

This conclusion seems valid also for other nodular limestones in the P ieniny Klippen-Belt 1.

A g e o f t h e L o w e r N o d u l a r L i m e s t o n e

As to the age of the Lower Nodular Limestone, the following data are available.

In the lower p a rt of th e Lower Nodular Limestone in a klippe near the village Niedzica have been found ( B i r k e n m a j e r and Z n o s k o , 1955): Coenoceras calloviensis (O p p .), Parkinsonia sp., pro parte ex gr.

parkinsoni (S o w.), pro parte cf. calloviensis (L o c z y), Cadomites sp.

pro parte cf. C. rectelobatum (H a u.), Phylloceras cf. viator (D’Orb.), Ph. kudernatschi (H a u.), Calliphylloceras disputabile (Zitt.), C. cf. dispu­

tabile (Z i 11.), Nannoly toe eras tripartitum (R a s p.), etc. This fauna indicates the highest Bajocian? — Bathonian — Callovian age. In the same klippe Laevaptychi occur exclusively in the upper p art of the Lower Nodular Limestone. Laevaptychi appear somewhere betw een the macrocephalus and lamberti zones.

In the Lower Nodular Limestone in a klippe of the P ruske Series (equivalent to the Niedzica Series) in the valley Podhradska in W estern Slovakia, have been found (A n d r u s o v, 1953, p. 38 (350)): Phylloceras kudernatschi (H a u.), Nannolytoceras tripartitum (R a s p.), Cadomites rectelobatum (H a u.). This fauna indicates a Bathonian-Callovian age.

In the Czajakowa Skala in the lower p art of the Lower Nodular Limestone (a) have been found some Phylloceratids, Lytoceratids, P eri- sphinctids and Cadomites. They have not been more exactly determined, but they seem identical w ith the ammonites from the klippe near Nie­

dzica listed above. The lower lim it of the Laevaptychi is sim ultaneous w ith the contact of the m iddle (b) and th e upper (c) parts of th e Lower Nodular Limestone. It seems therefore th a t this p a rt of the Nodular Lower Limestone in Czajakowa Skala w hich contains the exotic frag­

m ents is of a Bathonian age.

1 A n d r u s o v , 1953, p. 22 (334) and p. 44 (356) ■considers lall the n o d u la r lim estones in the Pieniny K lippen-B elt as b ath y al sediments.

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MODE OF TRANSPORTATION OF THE EXOTIC FRAGMENTS

We shall assume th a t all the above described eixotic fragm ents have been transported into the Lower Nodular Limestone sedim entary region sim ultaneously and in the same way. In view of w hat was said above, this assumption seemed quite justified.

Volcanic eruption is a possible transporting agent. Nevertheless it m ust be excluded as no traces of volcanic activity have been found in the Dogger of the P ieniny Klippen-Belt.

Turbidity currents and subm arine slumps can tran sp o rt great rock fragm ents from the littoral to the bathyal or abyssal zones. However, the extrem e scarcity of coarse clastic m aterial and the lack of graded bedding and other significant features (cf. K u e n e n, 1953, K s i ą ż - k i e w i c z, 1954) in the Lower N odular Limestone lead us to the exclu­

sion of a turbidity cu rren t or of a subm arine slum p as the transporting agent of our fragments.

Drifting ice can easily transport rock fragm ents over great distances.

Lack of striae on our fragm ents does not exclude th e ir glacial origin, as the percentage of striated fragm ents in glacial sediments is someti­

mes very small (cf. W e n t w o r t h fide P e t t i j o h n, 1949, p. 57). It seems, however, th a t the climatic conditions of th e tim e would not have allowed the form ation of glaciers. No evidence of glaciation has been found in th e whole Jurassic of the Tethys region (A r k e 11, 1956).

On the other hand, th ere is evidence of a ra th e r w arm climate. It is only in California th a t Jurassic tillites have been found (fide Umbgrove, 1947, p. 261, Fig. 161). A r k e l l , however, does not m ention them in his monograph of the Jurassic (op. cit.).

T hat our fragm ents - are not gastrolithes appears from the lack of glaziness (cf. Abel, 1935, pp. 310—317). T hat they have been inadver­

tently swallowed seems improbable in view of th eir size (65.7 kgs.) 1.

Rafting of rocks by algae is another possible transportation agent.

It seems, however, th a t our fragm ents weigh too m uch for such a mode of transport (for bibliography vide E m e r y , 1955; S h u m w a y , 1956).

D rifting wood or „floating islands” of tangled grow th can travel over great distances. They m ay carry in th eir roots fragm ents of rocks. The subject has been recently treated by E m e r y (op. cit.). The most im ­ pressive of the m any instances m entioned by this author are the follo­

w ing,,..^ kauri tree afloat in the Gulf of Papua. This tree was three metres in diameter... Held by its roots was a boulder three or four m etres in diameter... The sighting was about 150 miles off the Fly River, which was probably the source... The tree had been in th e sea long enough, however, for boring organisms and barnacles to become esta­

blished”, and „...pines a m eter in diam eter cast ashore on Nonouti Island th a t carried by th eir roots stones of fine-grained basalt of all sizes;

he (H a r t z e r) believed th at the trees came from New Zealand 1200 miles aw ay” (op. cit., pp. 52—53).

1 F o r bibliography on tran sp o rtatio n of rock fragm ents by anim als vide E m e r y (1955), and F l e m i n g (1951).

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The Middle Jurassic Coniferous trees seem to have been quite able to hold by th eir roots rock fragm ents of such a size as ours (65.7 kgs.)

and to drift despite this encum brance for a long time.

It seems therefore th a t the following mode of origin of our frag­

m ents is the most probable. A tree, or a mass of sm aller plants, growing upon an alluvial deposit, containing entangled in its roots our rock frag­

ments, has been torn off by a flood. Subsequently it has been carried to the sea, w here it drifted for some time. W hen putrefaction advanced sufficiently it sunk and our fragm ents have been deposited on a small area of the bottom in the Lower Nodular Limestone sedim entary region.

MACROCLASTIC EXOTIC FRAGMENTS IN THE RADIOLARITES AND IN THE BIANCONE IN THE PIEN IN Y K L IP P E N BELT

As in the Lower N odular Limestone, so in the other nodular lim e­

stones, in the radiolarites and in the biancone in the P ieniny Klippen Belt macroclastic exotic fragm ents are extrem ely rare. It is impossible to determ ine th eir density per square kilom eter of the bottom, b u t some idea of th eir scarcity m ay be obtained if one considers th a t th e first author has inspected m any thin plates and m apped the P ieniny Klippen Belt for eight years, and the second author has collected fossils from the rocks in question for three years, and the only macroclastic frag­

m ents found — besides the fragm ents from Czajakowa Skała — are the following:

1. Quartz, pale blue, opaque, well rounded, 1.2 X 1.0 X 0.9 cms., enclosed in the m arl betw een the nodules, passage beds betw een the Pseudo-Nodular Limestone (Kimeridgian) and the Biancone (Tithonian- Barremian), Branisko Series, klippe Stronia in the P ieniny Mts.

2. Quartz, colourless, transparent, subangular, 0.4 X 0.3 X 0.2 cm., on the surface of a layer 1, Green Radiolarites (Upper Oxfordian) 2, Nie­

dzica Series, Buwałd klippe in the valley Kosarzyska near Falsztyn in Spisz.

3. Quartz, white, opaque, well rounded, 0.13 X 0.13 X 0.07 cm., on the surface of a layer, U pper Red Radiolarites (Upper Oxfordian) 2, Niedzica Series, klippe Pod Czerwoną, valle of the Skalski stream near Jaworki.

4. Quartz, green, transparent, subrounded, 0.5 X 0.4 X 0.4 cm., on the surface of a layer, G reen Radiolarites (Upper Oxfordian), ² Branisko Series, klippe on the SW. slope of the m ountain Flaki, P ieniny Mts.

5. Cristalline schist, fine grained, dark rose, angular, ⁰.⁸ X⁰.⁶ X^{0 . 6} cm., on the surface of a layer, Biancone (Valanginian-Barremian), Branisko Series, quarry near the road from the bridge on the Poprad to Ujak (Czechoslovakia).

Both radiolarites and biancone are, in the Pieniny K lippen Belt, pelagic and deep sea sediments (cf. S u j k o w s k i , 1932, A n d r u s o v , 1953). Macroclastic exotic fragm ents listed above m ust have derived

1 It has >not been .possible to distinguish betw een the low er and th e upper surfaces, as all! the exotics listed here have been found enclosed in loose fra g ­ m ents of rocks.

2 U pper O xfordian in A r k e l l ’s (1956) sense.

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either from land or from the littoral zone. The mode of their transpor­

tation could have been th e same as th a t suggested by us for the exotic fragm ents in the Lower Nodular Limestone of Czajakowa Skala (vide supra), or they could have been rafted by algae to m off by wave action.

Obviously eolic transport m ust be excluded.

It can be suggested here, that, in view of w hat has been said above about the macroclastic ©xotic fragm ents in the pelagic and deep w ater sediments in the Pieniny Klippen Belt, the fragm ents of silicified wood found in the radiolarites in the Schistes Lustres zone of the Alps and in the D inantian radiolarites in Southern France (fide G i g n o u x , 1950, p. 401, n. 3) should not be accepted as evidence of a near shore and shallow w ater origin of th eir respective enclosing rocks.

It could be also suggested th a t the exotic fragm ents contained in the Bathonian limestones of th e High T atra Series between Wielka Swistow- ka and Mala Swistowka in the T atra Mts. ( P a s s e n d o r f e r , 1951, p.

51) and in the Albian glauconite limestones of the High T atra Series in the T atra Mts. ( P a s s e n d o r f e r , 1930, pp. 369—370, 533— 535; 1951, p. 75), have been transported into their enclosing sediments in a sim ilar way as the exotic fragm ents from Czajakowa Skala.

PROVENANCE OF EXOTIC FRAGMENTS FOUND IN CZAJAKOWA SKALA

The presence of certain rock types among our fragm ents, and the relation betw een the num ber of fragm ents of certain rock type and th eir volume (Table 3), m ust have been controlled by the abrasion agent 1.

This m ust be taken into account w hen using our fragm ents in palaeogeo- graphic considerations.

The petrographic character of our fragm ents implies th at the sim­

plest possible structure of the land they derived from m ust have been th e following. There was a cristalline massif containing muscovite, bio- tite, and muscOvite-biotite gneisses and gneissoid granites. It was in tru ­ ded w ith aplites in its low er part, and w ith various subvolcanic porphy­

ries: m icrogranitic and micropegmatitic quartz porphyries and w ith gra- nophyres in its upper part. W ith these intrusions w ere connected th e extrusions of felsophyres and of porphyric tuffs. As all these m agm atic rocks are comagmatic, they have probably been formed in the same cycle of magmatic activity. Both the cristalline schist massif and the magmatic rocks have been covered by sedim entary rocks represented among our fragm ents by a piece of limestone.

If we assume th a t our fragm ents derived from w ithin the central or

1 I f w e are rig h t in suggesting th a t our fragm ents d eriv ed from riv e r deposits, comparisons w ith the selective abrasion of p resen t rivers could give some idea of the lenght of tran sp o rt. F o r exam ple, in th e u p p er course of th e riv e r Dun'ajec, fragm ents of m ica-sehists p ersist o v er the distance o f 3 km., of am phibolites — 35 km., of lim estones — 50 km., of gneisses — 90 km.; a fte r 90 km . rem ain only w ell rounded fragm ents of quartzites and of granites. G enerally speaking, all rocks of sm all resistance a re practically elim inated over the distance of 35 km.

( U n r u g , 1957). It seems th a t our fragm ents have not been tran sp o rted by a riv e r over a long distance.