Lower Cenomanian trace fossils and transgressive deposits in the Cracow Upland

acta geoIogica polonica

Vol. 21, No. 3 Warszawa 1971

Lower Cenomanian trace fossils and transgressive deposits

in the Cracow Upland

ABSTltACT: iLower Cenonumian abrasion surfaces of ;the CrIac.ow UiPland aJbound in boll"1ings of lithophag,s such as sponges, ipdly.chaetes, pe1ecypods and echino.itds. Of many trace fossils OClCUrring· in ,these surifaoes, the fO'l'llXl_ Pseiuropolydorltes radwan- skii ichnogen. et ichnosp. nov., attriJbutable

to

polychaetes, bas 'been established as

a new <lne.

IJNTI'.ROIDUCI1IDN

During the studies on the Mesozoic deposits of the Central Polish Uplands, the writers paid their attention to the transgressive Cenomanian deposits occurring in a few outcrops near Cracow (Fig. 1). Especially were studied the Cenomanian abrasion surfaces in which numerous bo- rings of lithophags had for the first time been found.

The writers' stratigraphic considerations have been aided bya col- lection of the Cenomanian ammonites from Iwanowice, housed at the Polish Academy of SCiences, Museum of the Earth, and which was made available for the studies by courtesy of Dr. S.

M~czyflska.

Sud6l

The outcrops of the transgressive Cenomanian deposits at Sud61, des-

cribed for a long time, aTe of a fundamental importance for the strati-

graphy of this stage in the environs of Cracow (ZarE:Czny 1878, 1894; Pa-

434 JERZY Gl.AZEK, RYSZARD MARCINOWSKI & ANDRZEJ WIERZBOWSKI

C

Olubnia

7.0 [ .

a~~m

E

^Suddll

. ~

'. :

: .

: :

. .

:

Fig. 11

iLo'Cation.Qif the investiga1ed profiles

[.:::::,:::J4

~5-5

Gl~2~3

o

Wifkowice

A Position of the area in Poland. B Geological sketch-map (after Gradziilski 1960) snowing situation· of the described profiles: a Upper Jurassic, b Upper Cretaceous, c Tortonian, d investigated abrasion surfaces, e faults, f occurrence Site of the Lower· Cenomanian ·ammonites at Iwanowice. C Profile in the Dlubnia valley, D Profile. at WitkJOwice, E Profiles at Sud61 Upper Jurassic: 1 limestones, 2 marls; Cenome.nian: 3 conglomerates with intercalations of sandy limestones, 4 sandstones; 'Senonian: 5 marls; 6 Cenomanian abrasion surface; 7 borings

of pelecypods; 8 borings of polychaetes; 9 burrows of decapod crustaceans

now 1934; Bukowy 1957, 1960a) .. The most important profile occurs in a now filled up quarry (Fig. 1B, locality 1). In 1970, this profile has been exposed by the writers by dug holes (Fig. lE).

In this profile, deposits of the Upper Jurassic submarine slump, consisting of marls and blocks of butty limestones (Glazek& Wierzbow- ski 1972) are truncated by a flat Cenomanian 'abrasion surface, which

LOWER CENOMANIAN TRACE FOSSILS 43'5 .

displays various traces of the life activity, strongly differentiated

. and

depending on the type of the substrate.

In the marly substrate, these are the burrows filled up with the Ce- nomanian material. Most numerous of the burrows has a tubular forked appearance, and such forms were described by

Zar~zny

(1878, Table IV) as "Scyphia sudolica". These are most similar to Thalassinoides Ehren- berg, 1944, which are interpreted as a result of life activity of the deca- pod crustaceans (HantzscheI1962, Kennedy 1967).

In the limestone substrate, these are very numerous borings left by various organisms (PI. 1, Fig. 1) which are described in systematic part of the present paper. The borings of sponges (Entobia Bronn, 1837, emend.

Bromley, 1970),

poly~haetes

("Potamilla Malmgren, 1867"; Pseudopolydo- rites radwanskii ichnogen. et ichnosp. nov.), pelecypods and echinoids (PI.

1,Figs 1 and 2; PI. 2, Figs 1-4) have been · determined. These borings are abraded to a varying degree, but frequently superposed what points to several generations of the lithophags.

The limy conglomerate (lower conglomerates of

Zar~czny,

1878, 1894; Panow 1934; Kamieiiski & Piqtkowski 1950), c. 10 cm in thickness, overlaying the Upper Jurassic marls, is the oldest Cenomanian deposit.

This is of the pUddingstone type with larger pebbles of black, slightly rounded flints reaching 8 cm in diameter and smaller, well rounded pebbles of quartz to 2 cm in diameter. An abundant matrix consis'ts mostly of the psammiti'C quartz material, together with glauconite and a considerable amount of heavy minerals. These gravels penetrate into the Thalassinoides burrows. The conglomerate does not occur on abraded limestone blocks, instead there are only single

quar~z

pebbles in sandy infillings of the lithophag borings. The inrillings are considerably enriched in heavy minerals, among which garnet, magnetite, amphiboles or pyro- xenes and glauconite have been stated. Fragments of a silicified Juras- sic fauna (crinoid debris, echinoid spines) are also met with. The walls of borings are pitted by sand grains (cf. Radwaiiski 1965b).

A slightly cemented sandstone, either gray or secondarily stained by iron compounds, with its thickness varying between 1.2 and 2.3 m overlies the abraded Upper Jurassic limestone blocks and the lower con- glomerate

(Zar~czny

1878, 1894; Bukowy 1957, 1960a).

Higher up, indistinctly separated from sandstones, there occurs a layer of strongly limy conglomerate, c. 1 m thick (upper conglomerates of

Zar~czny,

1878, 1894; Panow 1934; Kamieiiski & Piqtkowski 1950). The upper, much the same as

.

lower 'Conglomerate is of the pUddingstone type but it is characterized by a smaller amount and grain-size of the clastic material. A fairly numerous fauna is recorded in this layer

(Zar~czny

1878, 1894; Panow 1934).

These beds are overlain by marls attributed to the Senonian (Panow

1934, Bukowy 1960a).

4136 JERZY G;t.AZEK, RYSZARD MARCINOWSKI & ANDRZEJ WIERZBOWSKI

Batowice-Sud6l railroad station ·

Traces of abraded pelecypodborings may be found in the abrasion surface truncating the Upper Jurassic limestones in now abandoned quarries situated near the Batowice railroad station (Fig.

1B,

localities

11

and

Ill).

Higher up, there

^'axe

conglomerates with quartz pe'bbles (Buko- wy 1960a) Similar to the lower conglomerate from the outcrop described above.

Witkowice

In , the village Witkowice, a set of quarries (Fig.

1B)·

in which Upper Jurassic limestones are truncated by a fairly even abrasion surface, stret- ches on the easieTn edge of a deep valley of the Garliczka stream. Irregu- larly distributed'borings of lithophags occur on this surface. In the nor- theastern outcrops, only rare, strongly abraded, probably pelecypod bor- ings may be observed on the abrasion surface. In the western part, this surface displays excellently preserved (PI. 1, Fig. 3 and PI. 2, Fig. 5) single borings of pelecypods of the genus Myopholas Douville, 1907. In the sou- thern part, the abrasion surface abounds in borings of polychaetes "Po- tamilla Malmgren, 1867" and pelecypods.

The abrasion surface is covered with a limy conglomerate, composed of well rounded, flat quartz pebbles reaching 4 cm in diameter, and the lay€T 'being up to 0.7 m in thickness

(Zar~czny

1878, Bukowy 1956). In the western outcrops, a wedged-out intercalation of sandy limestones (Fig.

1D)

occurs in the lower part of the conglomerate. The conglomerate is overla!i.n by Senonian marls (Bukowy 1956).

Dlubnia valley

On the slopes of both edges of the Dlubnia valley, the Upper Juras- sic limestones, truncated by a relatively even a'brasion surface (Fig.

1B),

are outcropping, along the distance of c. 4 kms, between Iwanowice and Maszk6w.

In the northern outcrops, a well-known locality is situated near Iwanowice from which the Cenomanian fauna was collected (Panow 1934, Ml:lczynska 1958,

cf.

also Kamienski

&

Pil:ltkowski 1950). As a resu}lt of the writers' studies another profile has been stated on the eastern edge of the valley between Poskwit6w and Maszk6w (Fig.

1B).

The outcrops with the abrasion surface begin south-west of the

mouth of a ravine descending from the village Slomiana. In this locality,

the limy Cenomanian conglomerate, composed mostly of quartz pebbles

to 1.5 om in diameter, overlies the Upper Jurassic limestones, truncated

LOWER CENOMANIAN TRACE FOSSILS 437

by an abrasion surface. Dark phosphorite concretions, also up

to

1.5 cm in size occur in this conglomerate.

Abraded pelecypod and polychaete ("Potamilla Malmgren, 1867") borings, and frequent diagenetic pits (cf. Radwanski 1965b) of quartz pebbles, occur on the abrasion surface. Mar Is, usually assigned to the Senonian, overlie the conglomerate .

. In a large quarry, about 300 m further to the west (Fig. 1C), -the

Upper Jurassic limestones are truncated by an abrasion surface bored by a similar assemblage , of pelecypods and polychaetes (PI. 1, Fig. 4).

The surface is overlain by a layer of the Cenomanian conglomerate, c. 1 m thick, and composed of scattered, flat and well-rounded quartz pebbles to 3 cm in diameter, large pebbles and fragments of Jurassic flints, rea- ching 8 'cm in diameter and, finally, similarly sized dark-gray phospho- rite concretions. The echinoid Pyrina laevis Ag. and crinoid debris are

to be found in this conglomerate. The green ,colour· of the sediment and.

a green substance (glauconite?) coating the abrasion surface and some of the pebbles is a very characteristic feature of this layer. A micritic matrix with foraminifers has been stated in thin sections here. The p,eib- bles are mostly of metamorphic quartzites, less frequently vein quartz and larger, poorly rounded flints. A fine quartz sand with an admixture of glauconite occur in the conglomerate along with the

^~ebbles.

On the whole, the conglomerate resembles the upper conglomerate from Sud61, described by Kamienski

&

Pil:j,tkowski (1950).

S'illtA T.lIGRAlPHIC ;pjOO]'I1]QIN

According to the previous authors (panow 1934; Bukowy 1956, 1960a; Alexandrowicz 1960b), the deposits, which overlie the abrasion sur- face under study, belong to the Cenomanian. The older Cretaceous depo- sits in the Cracow Upland do not occur in the profiles studied by the writers and, met with here and there, they only fill up the depressions in the Jurassic substrate. These are · sands devoid of fauna and conven- tionally assigned 'to the "Vraconi'an" or Uppermost Albian (panow 1934;

Bukowy 1956, 1960). The Cenomanian deposits in the Cracow Upland were subdivided by Panow (1934) on the Ibasis of the Sud61 profile (cf.

Fig.

lE).

The conglomerate, directly overlaying the Jurassic deposits, with Parahibolites tourtiae (Weigner), was assigned by Panow to the Lo- wer Cenomanian

^1.

The oveTlaying sands and sandstones devoid of fauna

1 In add,ition to the outc!rops 'under s>1:udy, conglomell'ates from Korzkiew, con- taining Pecten asper Lam. (cf. Panow 1934), have als,o- been art;tributed to the Lower Cenomanian. This pelecypod ~s" however, knOlWn f!rom various

!Parots

of the Ceno- manian and .iiflg Oc<:'UTl'ence depends on the facl'a'l. developmen,t (Hantzschel 1900, Tri:iger 0000).

438 JERZY GLAZEK, RYSZARD MARCINOWSKI & ANDRZEJ WIERZBOWSKI

were regarded as transition beds between the Lower and Middle Cenoma- nian. The cephalopods Schloenbachia varians (Sow.), Baculoides baculoi- des Mant. and Scaphites aequalis Sow. were regarded by Panow (1934) as documenting the Middle Cenomanian age 'of the upper conglomerate.

The Cenomanian deposits occurring in other discussed profiles (Wit- kowice, Iwanowice) were, mostly on the basis of lithological criteria, correlated with the upper conglomerate from Sud61 and, consequently, considered as Middle Cenomanian (panow 1934, Panow in Kamienski &

Piqtkowski 1950). The Cenomanian deposits from the Dlubnia valley, south of Iwanowice (cf. Fig.

le)

are also similar in lithological character to those from Witkowice and I wanowice.

In all the profiles elaborated, the deposits, recognized thus far to be the Middle Cenomanian, are overlain by marly deposits attributed to the Senonian.

The ammonite fauna, oollected from the conglomerate at Iwano- wice (Fig.

1B)

which has so far been

ass~gned

to the Middle Cenomanian (Panow in Kamienski & Piqtkowski 1950, Mqczynska 1958) is represented (the Museum of the Earth's collection, numbers Mz VIIIIMc-1301-1304) by the follawing species: Schloenbachia cf. varians (Sow.), S. subvarians Spath, S. subtuberculata (Sharpe), S. ventriosa StieI.

In the bipartite division of the Cenomanian, widely applied in Po- land (cf. Cieslinski 1959, 1965; Marcinowski 1970), these species occur in the Lower' Cenomanian, Schloenbachia varians Zone (Wright

&

Wright 1951). In the tripartite division of the Cenomanian (Hancock 1959, Ken- nedy 1969), all the above listed species of Schloenbachia, are known both from the Lower and lowermost parts of the

'Middle Cenomanian. At pre-

sent, there are no paleontological evidences indicative of the younger members of the Cenomanian

in

the environs of Cracow. The age of the conglomerate from Podg6rze and. Pychowice, considered by Panow (1934) as Upper Cenomanian on the basis of Orbirhynchia cuvieri (d'Orb.), is rather debatable, si'nce this hrachiopod is known from the Cenomanian through the Santonian (E. Barczyk in Marcinowski 1970) .

.

As follows from the presented stratigraphic - considerations, all abra- sion surfaces with borings, are of Lower Cenomanian (in bipartite divi- sion) age.

SYSTEMATIC DElSORIPTI1JOtN OlF LI'IlHOIPHAG'S

Sponges

(PI. 1, Fig. 1; PI. 2, Figs 2-3)

IBo!l"ing,s of sponges are among ralI"e forms and have been found only at Sud61.

They represent the ichnogenus Entobia IBronn, 1'837, which, acc-oroding toO Bromley (1'970), corresrpo.nds to the boxings of sponges of the famUy Clionidae. Due

to

a rat-

LOWER CENOMANIAN TRACE FOSSILS 439

her PO'OIr sta,te of preservatdon and ,the Iac'k of a' ,co:mpalr,ative material, a m'OIfe de- tailed deteTmina,tion of these bOlriIllgs to the rank of khno,speoCies is 'iimpossible.

The borings stretch aver a few square centimetres and fOlfm a sy'stem 'Of closely s.pa'ced, fine,. 'ilfregU'Iarly shaped ga[Ielrie,s (0.3--'0.8 mm in diameter). It is difLicult to estimate to what an eXften,t the pattern od: g.al1e!l'iies visible is an ori- ginal system and to what an extent it might have been destructed. Surely, hewever, thlis could not be 'a system with extremely l'arge ch<8lll1lb&s, 'a% in Entobia cretacea fJiOJ:.tiock (cf. Bromley HlI70'). A system of smahl berings belonging to the ichnegenUiS Entobia and much mOire tSimi'lar to OU'lf specimens W1lJS dEIS,cribed by Stephenoon (119512) as Cliana ret.iformis from the Cenomanian of Texas. The Texan borings are, however, 'Of a coIllsp.kuously "camerate" type. A pal'tdcul,ar'ly slj;r·ong ,similarity to OU'lf spec<imens are displayed by the bOlfings of Entobia descroibed by Roniewicz (1970) as CUothosa sp. fwm the iEocene of the Ta,tra Mt6.

Polychaetes

TulbulalI' ,and U-shaped .borings" in aU pir'olbabd1i!ty attributable' to po[ychaetes, belong to ,the most frequent forms occurrling in the materiaJ. under study. The tUlbular borings have been ddentdfied as "PotamiHa J.VIaLmgren, 1'867", while U-sha- ped onelS represent a new ichnogenus PseudopoZydorites. The former have been found at Sud61, Wiltlrowlice and' in tlhe Dluibinia V'alley, the latter only at Sud61.

"Potamilla Malmgren, 1867"

(Fig. 2;

PI. 2, Figs la-b)

The name "PotamiZZa;Y in ichnoZogy. - The borings, 'bein,g described by var- ioue authors in 'the f'olSsi'l state and mO'rpho[ngtcaIly comparable to bordngs of the Recent Saibellid po'iychaetes of the genus PotamiHa OIl' species PotamiZZa reniformis (Muller) were usually named the lSIame as these latter ones. Such PotamiZZa borings were descrilbed from :tlie .o.vCiddle Jur~ssic ,of !We.stern EuiI'ope ([Holder & Hollmann 1,969) and those of PotarniZZa reni!Ormisi(MuIQer) from the Rhaetic and Lower JUT'alSi3k o[ Ithe TatiI'a- Mts (Rad'WlatiJskd 1'9'59): Pal~ogene of the Paris' Bas'in (Elle.nberger 1,947), Eo'ce:.ne of the Tatra iMts (Roniewicz .. 'l,g,66, 11917ⁱO) and Miocene of the Holy Cross Mts ~Ra'd":,,,a:6ski 1<!!169, 1!91710 ,~nd earlierwor'ks therein referenced).

Cel'oiain doubts may sometimes be _aroused bY_.the .relatin~hip of these fossil berings and the REcent genus' PotamiZZa. Th'Ls parti'cU'la.rly ,c:oriCelfns the Rhae'tk - Middle Jurassic borings. Some of rsuch bOIri,rtgs; dets~i:bed' by HOLder & Hollmann (1969) as PotamiZZa frlQ.m the Middle JU'lfassic \arE! so liittle'char,a'ctell'i'stic that they ar,oU'se doubts whether they come . fr,om the poly~haete,s'or phor,onids (cf. Voigt 1'97¹0).

Under s'uch cLrcums,t'anc€lS,' the_ writ errs decided.- in treference to the Ceno- manian ib<orings under study which are similar to those ,of - PotamiHa - to use quotation marks wJth the name and thus to emphasdze its more ichnoJ.ogical rat- her then wolOigical charalCiter.

In future, the necelSsdty wdll probably ardse to intrr:oduce a new ichnogenerioc name deitell"IIlining the ,,Potamtzza" boriings. There is aLso ,a possdbility of extending the IdllIlits of already existing ichnotax,o,ns. Here, we may mention ,that the horings called the Trypanites Miigdefxau, li9.3,2, are very sdmilaa: to s'ome bor,ings of the

"PotamiZZa" ttype (cf. HOlder & Hollmann 19169, Voigt 1970).

440 JERZY Gt.AZEK, RYSZARD MARCINOWSKI & ANDRZEJ WIERZBOWSKI

Material. - Three typea of the "Potamilla" borlings, desigrrated in the present papell." !by S'llccess['Ve letters

of

the aJpih:abet, ooou1' in Hie iLO'Wer Cenomanian ,abrraiSion suxfaces undell." study.

,JPotamiHa" type A l(iFigs Za-c and 2f-g). Blindly terminated tubular borings about 2.5

to

5 cm long, round in sec'tion, between .1: mm a,nd nela1'ly 3 mm in diameter and variously, iSOIlletames shMply Wlinding a few times. Some {)[ the bor-ings ,,Potarmi;Ua" type A begiinat the end of a "Potamilla" type B .boiL"ing (Fdgs 2f-g). 'I1he "PotamiHa" type A bodngs' iresemble those descrjJbed as PotamiUa reniformis (MUller) from the Rhaetic (Radrwaillskd 1009, Fig. 9), PaJleogene l((Ellen- berger 1-947, Fdg. 7D) and M1'ocene (Radwailsiki 11969, Fig. 2), as well as s,OIIne of Trypanites Ifil'Dm the Muschelkallt (Mililer 1006, E1ig. 2) and iK:immell."id'gian (Kazmier- czak & IPszc.z6l:kowBki 1968, IDig. 5) ..

a

o

---

b

o

1I

..

,I

"

11 11 1/

/1 11 //

11 //

\\ ,~,

"

^,~,

c

o

d e

00 ^{.0 f}

~tp!.

^..

s·· .~. ~ .. ?

Fig. 2

&r1ngs ,of polychaetes '~PotamiHa" at Sud6J:

a-c borings of "Potamttta" type A; d-e borings of "PotamiUa" type B; f-g borings of

"PotamiUa" type A developed in borings of "Potamitta" type B; h--i borings of "PotamiUa"

type C; j boring of "Potamitla" type C developed in a bigger (older) boring of the same type

ACTA GEOLOGICA POLONICA, VOL. 21 J. GLAZEK, R. MARCINOWSKI &

A. WIERZBOWSKI, PLo 1

Lower Cenomanian abrasion surface on the Upper Jurassic limestones at Sud61. The

boring~ are: a - Entobia, b - po·lychaetes, C - pelecypods, d - echinoids.

Borings in Upper Jurassic limestones (Ja) covered by Lower Cenomanian sands tones (C) at Sud61.

3 Borings of Myopho!as in Upper Jurassic limestones (Ja) covered by Lower Cenomanian conglomerate (C) at Witkowice.

4 Borings of pelecypods and polychaetes in Upper Jurassic limestones (J 3) covered by Lower Cenomanian conglomerate (C) at Dlubnia.

ACTA GEOLOGICA POLONICA, VOL. 21 J. GLAZEK, R. MARCINOWSKI &

A. WIERZBOWSKI, PLo 2

la-b - Two sides of the same section of "PotamiUa" type B (cf. Text-fig. 2d) and opening of

the boring Pseudopotydorites radwanskii ichnogen. et ichnosp. novo (cf. Text-fig. 3c);

Lower Cenomanian, Sud61.

2-3 Entobia; Lower Cenomanian, Sud61.

4 Pseudopotydorites radwanskii ichnogen. et ichnosp. novo (ho!otype, cf. Text-fig. 3a);

Lower Cenomanian, Sud61.

Borings of Myophotas; Lower Cenomanian, Witkowice.

All figures of na t. size

LOWER CENOMANIAN TRACE FOSSILS 441

"PotamiHa" type B (Figs M-g; PI. 2, Fdgs la-b). Blindly termmated tuDulaJ.'"

bo:riings about 3 to 5 cm Joog, round in section and 'about 4 to 6 :mm in diameter.

These borings aTe almiQS'I; completely stto:-aiJght, rarely verttilcal, mostly 'lWl"anged obliq,uely to an abrasion s1.U"face. Borings with much the same diameters, identified as PotamiUa reniformis OMiiller) were described fr·om ,the iPaleogene (EUenberger 19417j.

"PotamiHa" type C 1(IIDigs .2h-j). Bildndly te:rmlinated tuIbuJ.8lI." lborings between 1:2 to more than 115 cm long, round lin section and between 2 and 6 mm ii:n diameter.

The borings: are 'aB a Il"ule' s1Jriongly, OOIlDettimes a few times wii:nddng. FadJ."'ly long secJto!rs stretching approxliJmately hotrdwntaliy a!re chail"aC'terdSltic feature '00 the1rs.

Due to the di.s1fin.ct wdnddng of the bottiings, the aibrasdlVe 1Irunrcation ,causes g'ometimes the ~OTllDaMon of wideily open a'nd fairly iShallow, U-iShaJped' forms, ,(Fig. '2:3). Now and then, y'OIUIlliger ,J:)orings' of Ithe. ,,Potamil/Ja" type C begin at the po,intiS of deflection of oldelr- Ibioiings '(.Fig. 2;3). ~here Me also Iborings [ocalted in the boirings of pe1ecypods. 'Dhe tubu[3[" boJ.'"iiIngs of the "PotamilZa" type C dtiif·fer from those of the type of Potami~Za descr,ibed so far in Itheir tendency to toII."Iln U.,shaped bends and J,n thedr dimensions, particulal"ly in thed1- longer length.

Pseudopolydorites ichnogen. novo

Type tchnospectes: Pseudopotydorttes radwansktt ichnosp. novo

Derivatton of name: after a seeming similarity to the ichnogenus Potydorites Douville, 190&.

Diagnosis. - The tubua,aa:', U-shaped iboring with a few,centimeters long limbs, the intelrSpace ,of whlich is, composed of iIlon-lrefWlOrlked rock.

Stratigrophic position. - LoWer Cendmaonian.

Remarks. - Pseudopolydorites distinctly dliffers from the dchnogenus Pol'lfdorites Douvd['le, 11908 in a 'different material of the !ldrob inters.pace. IIn Pseudopolydorites the dntempace is CdIXlpoSed of an QIl'.i;glinal, uon-revror,ked rock, whiie in Polyd()//"ites, whlich COINesponds t1;o 'the borings of some !Recent Po'lydora (P. hopluro and P. ciliata), the interspace is fonned !by the ma:'teri'al excavated from the iSides and ibese af the boriiIng. In all ldkeliihood, S'OIIle IOf the U -shaped bor~ngs"

descE'ilbed from the M1ddlle Jurlru!sic (iHOlider & HoNmann i1969) as Polydorites, have thek ;inltarspace composed of an oIrIiginat Tack and, 'Consequenttly, they Woould also beloong to the lichnogenus' iPseudopdlydorites ..

Pseudctpolydorites markedly dWers from U-sha,ped, fine C'alV'ities met within slheills and be\longling too 'the ,ichlnogenera Caulostrepsis Clarke, !1900, and Ostreoblabe Voigt, ,1965, which a1"e embed<idn,g forms '(CIf. !BIrom:ley 11.97'0).

Pseudopolydorites radwanskii ichnosp. novo (Figs

3a-c;

PI. 2, Figs.

la-b

and 4)

Hototype: the specimen presented in Fig. 3a and Pl. 2, Fig. 4.

Type horizon: Lower Cenomanian.

Type tocattty: Sud6l near Cracow.

Dertvatton of name: after the name of Docent Andrzej Radwanski (Warsaw University), an author of several ichnological works.

Diagnosis. - T.ulbulllm", U-IS:hlllPed bor.ings, pJ.'"obalblly leflt by polycnaetes, il"'ound

~n section and ,about \6 to 6 mm in diameter. The limbs of the U~shaped loop are usually 3 to 15 cm long, thIis length being same1lime& shortened as a resUilt of an a1brasion o(Fig.3c). The stpa'ce between the llrnIbs,. a!bloult; 1.,2 ,cm toL8 cm wide,

•

44:2 JERZY GLAZEK, RYSZARD MARCINOWSKI & ANDRZEJ WIERZBOWSKI

a) o ^b) o

c)

Fig. 31

U~shaped .:barings af polychaetes at Sud61

a-c borings of Pseudopo!ydorites radwanskii ichnogen. et ichnosp. nov., variously abraded (a presents the holotype); d superposed borings of either (?)Pseudopo!ydorites or (?)"PotamiUa"

type C (d1) and (?)"Potamma" type B (d2)

campased ,of an ariginal, nan-<reworked, salid r·ack. Boring openings on the surf.ace raund, without ,a funnel-like depress,iOon. In the ma'r-.opernng part, the limbs display a characteristic ded'lection.of theilr trace in relation to' the deeper parts af the ibaring (Fig,s 3a-b), which 'are situated in one plane.

Remarks. -The dhs'OlliSSe'd baringlS cannot be cansidared as a:birasi,vely trunoated booings of the "Potamina" 'type, which never Wsplaysuch clo·se1y spaced and deEp U -shaped lo,ap (cf. 'Fig"s ~h, j). CelMaJin daUlbtsmay only be aroUsed by the borings shawn in Fig. 3d. 'Dhey may be ~nterpreted as two forms superposed on ea,eh other as a result of the des.tructian of an intervening partition. The first U-shaped f.orm (Fig. 2d1 ), l·a.rgel! in di-ameier, ibelmlgs to the dehnogenUiS' Pseudo- polydorites or, which JJS les"s ld:ke-ly, representtS a very sharp bend of an abraded

"Potamilla" type C baring; the second straight farm, smaller in diameter (Fig. '3d2),

is probably "Potamilla" type B.

Pelecypods

(PI. 1, Fig. 3; PI. 2, ;Fig. 5)

Borings ill pdecypads are among f-requent fo-rtms, iiaund in >all the outcrops srtudied. A ,considerable maljmity acf them are strongly ,aib·ooded whdch makes the detElfmination ,af theJ!f fuN. shape impossible. NO' remains of the ib'OriIlg pelecypods have been found in all barings.

Same le"ss str'ongly abraded ba.rings from iWlitkaWliee (iP1. 1, Fi,g. 3; PI. 2, Fig. 5) are chara·cteristieally pear-.shaped, their Cihamiber ^p'a!fts 'geIltly pas1sing ,intO' a nedt,

LOWER CENOMANIANTRACE FOSSILS 443

whose upper pall't is, however, 'liIbl'as~vely truncated. A maximum diameter of the chamber v:ardes Ib~een ,L5 and 2.il? 'Cm, whii'le, a maxjmuan length of a preserved boring am'Ounts to c. 5 cm. :In all llikelihood, 'these borings may he dnterpreted 'as bellonging to the genUlS Myopholas iDoUJiJ'ilU!, IlIS:G7, which is known in the fossil state from :the Middle Juras'sLc through the' Upper Albian {Cox 1J~619). In Poland, bOTings of this genus were noted from, the Lower Kimmeridgian of the Holy Gross Mts

(KaZmier:c~a;k & PszczOlkoWiski 1968).

Echinoids

Not V€ll'y numerous 'and strongly destroyed rounded pillS (PI. 11, FiJg. 1) were found in the a:bras.Ion suria,ce at Sud61. Their diarneteramounts to c. 3.5 to 4 cm and depth to ^Cl. 1 cm. The walls o:f :pits are fairly stefp and bottoms slightly flattened. In some oases, Ithe bottom is not completely even and bears traces of reworked older horings I(af ?pelecypods).

The pits under study are similar li.ncharader to those bored by regular e'chinoids. Such borings have been noted in the fossil stJa!te from the Cenomaman of Rhinela:nd 1(lKahrs' 19j27) and lMiocene 'Of the Holy Cross Mts (Radwansiki 19165a, 19169, 197'0).

Of the many localities of Cretaceous abrasion surfaces, varying in age, which are known in the Cracow Upland (Dzulynski 1953; Alexan- drowicz 1954, 1960; Bu'kowy 1956), the borings were found only in the Lower Cenomanian surfaces.

Abrasion surfaces bored by lithophags were formed during the maximal development of 'the Albian-Cenomanian transgression, which gradually invaded vast areas of Poland

(cf.

Ciesliilski 1959, 1965) and which in the Lower Cenomanian, probably completely covered the Cracow: Upland. The studied Cenomanian littoral structures resemble to some extent the structures formed during the Miocene transgression onto the southern slopes of the Central Polish l.!plands

(cf.

Radwanski 1965a, 1968, 1969, 1970). However, considerable differences are also recorded between the littoral structures of these two transgressions.

All the Cenomanian abrasion surfaces described are flat and,

consequently, have the nature of abrasional platforms which are rare

among the Miocene abrasion forms (cf. Radwanski 1968, 1969).

It

may

be 'assumed that the Cenomanian transgression was marked

by

a more

intensive abrasional activity and, therefo,re, it more strongly levelled the

substrate, leaving only abrasional platforms, while the autochthonous,

limestone rubble was completely destroyed. A considerable difference

occurs 'between the materials covering abrasignsurfaces in the two

compared transgressions. The Miocene deposits containmostlyliuto-

444 JERZY Gl.AZEK, RYSZARD MARCINOWSKI & ANDRZEJ WIERZBOWSKI

chthonous material, whereas the Cenomanian ones are composed mostly of the allochthonous quartz gravel and sand. The clastic quartz material dragged by waving, played the grinding role which intensified the abrasive a'ctivity of waving. Sweeping the material has been confirmed at Sud61 by the lack of lower conglomerate on the limestones truncated by abrasion surface, while only single quartz pebbles and heavy minerals have been preserved as trapped in the lithophag borings.

The Lower Cenomanian assemblage of lithophags of the Cracow Upland differs from the Miocene assemblage in the lack of borings similar to those made by Recent Polydora, and in the presence of Pseudo- polydorites ichnogen. novo Both these assemblages display, however, a far-reaching analogies in the amount and systematic assignment of all remaining lithophags.

It should be added that the Albian,,-Cenomanian and Miocene transgressions entered an uneven limestone sU'bstrate, in the depressions of which older sandy sediments, reworked by the transgressing sea or deposited in the initial stages of transgression, have been preserved here and there (cf. Bukowy 1960b, Radwanski 1967, Baluk.& Radwanski 1968).

The littoral structures described are the result of Albian-Ceno- manian transgression, which gradually invaded the Meta-Carpathian arch, uplifted in the Lower Cretaceous (Glazek

&

Kutek 1970). Flooding this 'arch which comprised the Cracow Upland, by the Cenomanian sea broke, in the higher Cretaceous stages, the inflow of a considerable amount of the sandy material to the surrounding basins. The Cracow Upland remained, however, as a part of the rise which separated deeper sedimentary basins, that is, the Carpathian geosyncline in the south and the platform (epicontinental) :basin in the north. This

is

the reason why younger abrasional surfaces and many stratigraphic gaps are now met with in the Upper Cretaceous deposits of the Cracow Upland (cf. Panow 1934; Dzulyilski 1953; Alexandrowicz 1954, 1960; Barczyk 1956; Bu- kowy 1956).

_ The discussed littoral structures are a unique phenomenon in the Polish Cretaceous. Despite the fact that vast areas were covered by the Albian-Cenomanian transgression, no conditions were produced - except for the environs of Cracow - favourable to the formation of abrasion surfaces and appearance of lithophags. The occurrence of such a nume- rous assemblage of lithophags on the Cretaceous abrasion surface is also exceptional on a world-scale. The only occurrence of the Cenomanian abrasion surlace with echinoid and -?pelecypod borings known to the present writers is that in Rhineland (Kahrs 1927).

Institute

of

GeoZogy

of

the Warsaw University Warszawa 22, AZ. Zrwirki i Wigury 93

Warsaw, March 1971

LOWER CENOMANIAN TRACE FOSSILS 445

AiJEx.AINlDBJOWlICZ S. ,1.9154. Turon piOludndiowej cZE:sci IWyzyny KrnkowskJiej I(Turonia.n of southern part of the Cracow Upland). - Acta Geol. Pol., \1101. 4, no. 3. !Warsz.arwa.

1000. Budowa geologiczna okolic Tyiica '(Geological structua:e of the vicinity of Tyniec, Cracow region). - !Siul. Inst. Gecl.1<52. !Wal'5lZa.'W'a.

BAl.tUK W. & RADW ANSiKa: A. ,1968. DoIlnotorlOnskie piaskli w iNawodq;icach kolo lK.I.imonrt!owa, Lch fauna d. wyksz,tal'Cen,ie fuejalne (lnwer TortoIllian sands at NawodZlice, s'outhern <slopes· 'of the Holy Cross

Mts,.,

thel'!" <fauna and facial developmenJt). - :ACta Geol. Pol., wl. !l.'8, no. 2. Warsmrwa.

BAiRCZYK W. 111915i6. 0 rutworach gornok'l"edowych na Bonan:e pod Krakowem (On the Uptp€r Chalk de,po.sits on Bonarka near Cracow). - Studia Soc. Sci.

Tol'unensis, !Sect. C, vol. 3, -nil' .2. Toruii.

BROIMiIJEY !Et. G. :11970. iBor'ings as tmce-d:ossiJs and Entobia cretacea Portlock as an example. In: Crimes T. P. & Harper J. C. {Ed.), 'Trace i£osB.iis. - GeoL J.

(Spec. [ssue, no. 3). lLi<ver:pool.

BUlK.OWY S. 19:56. Gool'ogia OIbsml'lu pomi~y iKr:alrowem a KorzkwUi (Geology of the ~ea between Craoow and iKorzkwda). - Biu!.. Inst. Geal. lOO. Warszawa.

1007. iNowe dane 0 kimerydzie oIkolic Krakowa CNew data about the Kimme- ridgian in the v:ici1l!ity ·of Cracow). - iP'rzegl'ld Gee!., R. 5, nr 2. WarsZlawa.

11900a. Wydeczka !l. 7. iBatOwti.ce - Sud61. In: Przewodnik po okolicach iKrako- wa. Wydawn. Geol. 'Wal'szawa.

1,960b. Uwa'gi ,0 sedymentacji i diagenezie albuokolic Krakowa (Notes on seddmeDJta:tion and diagenes'is of the AWbian !in Cracow Il'egion). - Biul. I·ost.

Geol. 152;lWaIt'rSlZawa.

Cl'ESLlIN'SKJr

s.

H~59. Alb ti ce.IlJOIDaiIl polnocnego o'brzezen:ila Gor S~kr7Jyskirch

{The Albian and Cenoman!ian d,n the northern lPerJ.phery of Ithe SwiE:ty Krzyz Mountadns). - iP'irax:e TrnIsrt. Geoll.,

t.2B.

Wax!S'Zlawa.

li!l'65. St'ratYgll"afda i fuuna cenomanu J>olSoki, be.z: Karpat Ii SlClSka (Sbratigraphy and fauna of the Cenomanian in Poland, excluding the Ca'!"pathians and Silesia). - Biull. ILnsrt. Geol. ,1i92L lWarszawa.

COX L. iR. 19169. Family MyoPh,oladidae Oox, 1964. In: Maore R. C. (Ed.), Treatise on ilnrverteib!rate (pIaleonta1ogy, ,part N 'I)J.VIOOlusca6). !Jawrence.

DOUV:ruL:'€ H. 1907. iLes iLamlme1'L1biI'anches caV'ico.ies au Desmod:ontes. - iBu'll. Soc.

Geol. France,

m.

4, t. 7. Paris.

~ 1'908. IPerlorations d'Annelddes. - Ibidem.

DZUiL YN'SK!] S. 1953. Tektonika

1Pd.

cz~i Wyzyny iKrakows~iej (Tectonics of the southern pall't of the Cracovian Upland). - Acta Gool. lPol., vol. 3, no. 3.

lWarsmwa.

ELDENBERJGER IF. '1194'7. Le prolbleme Uthoilogique de l'a c:raie durcie de Meudon. - BUllil. Soc. Gaol. JF1rance.

ser.

^{5, \1101. J7.} J'aIt'ris.

GLAiZlElK J. & KUTEK J. 1970. The Holy CrOS'S' rMts area J.n the Alpine driastll'OIlhic cycle. - Bull. Acad. Plol. SoL, 1Ser. Sci. GeoL Geogr., vol. 1:8, no. 4. Varsovlie.

&: Wl'.ElRrZIJ30iWSK:I A. 197:2. 'iW sprawie rzelkomej tmosgresji kimerydu na Wyi.ynie iKrakowskiejCOn the allegedlKimmeridgian trans'gression in the Cracow Upland). - Acta Geol. iPol., ViOl. 22, no. 1 (in press). lV\1iarszawa.

GBJAlDZJINSKJI R. 19160. Mapa geologiczna Oikolic iKrakowa. In: Przewodni.'k geolo- giczny po okolicach iKrakowa. 'Wydawn. Geol. Warszawa.

446 JERZY Gl:.AZEK, RYSZARD MARCI~OWSKI & ANDRZEJ WIERZBOWSKI

HANCOCK' J. M. '1-900. Les ammondtes du Cenoma.nden de la Sadhe. - C.-R. du CongI'. Soc. Savantes Dijon 1009: Co'lloque sur le Cretace sUiperieur Franc;ais.

Dijon.

HkNTZiSCHEIL 'W. 1:£13.3. D3JS Cenoman und die Plenus·zone in der s'Udetischen Kreide. - tA'hh. Preuss.Geol.·'Landes'anst., iN. 'F .. , H. 15'0. Berlin ..

- 1962. 'Drace fossils and probJEmatdca. In: Moore R. C. (Ed.), Treatise on .]nvextelbr·ate lPaleontioiogy, ParttW {lMiiscellil.anea). Lawrence.

HOiUDER H. & HCiLl.JMAiNN oR. .1.009. iBohrl"gange ffiiwiner Cirganismen in jurasslschen Harlt- und FeLsboden. - N. Jib. Geol. lPaHiont. .Abh., Bd.' 1:33, H. 1. Stuttgart.

K.AH1RS E. 1'!li27. Zur PaHio.geographJie der Olberkn)ide in Rheinland Wes.tfalen. - N. JIb. Miner. Genl. IPaHionl, Bd. 518, Albt. B. Stuttgar,t.

-KAMIIlEN\slK[' !M. & 1P\I:1\'I!KOWSlKJE A. '119!5'(). iK:-ilka uwag 0 cenomanieokolicy lKra- kowa (Quelques. remarques sur le .Cenomanien des environs de Crac·ovie): - 1R0cz. P. T. Geol. (Ann. Soc. GeOil.. iPOll.), t. H~; 2. 3. iKrak6w.

KAZ'M:r:mRJOZAK J. & PSZCZOllKoiWSIK[ A. 19\68. Niecilu~)!Oscd sedymentacyjne w dolnym kimeryd.zJie poludniowo-za'chiodniego obrzezenia mezozoic-znego Gor SwiE:tokrzysikkh ,(Sed·im~!TItary disoontinuities dn Ithe Lower Kimmexidgian of

the HoJy Cross !Mts). - Acta Geol. Pol., 'Vol. ,1,8, no. 3 .. Wars:z;awa,

KEJNN'EDY IW. J.. ,1,9167. Burrows 'and rurtface i1;races from the l.Jo'Wer ChaJ:k ,of 'slOuth€T:n EngLand. - Bull. Birt. 'Mus. (Na't. Hist.) Geo1., vat ·1-5, -no. 3. London.

-li9I69 .. The correlation of the Lower Chalk of s.outh-east England. - Ptroc. GeoL Ass-oc., v·ol. 80, part 4. London.

MARJOIlNIOIWSKiI R. 1970. The Cretaceous· trarisgressdve deiposits ea..&1; of Cz~tochowa

.(fPolish Jura Cha~n). - A'Cta GeGl. PGl., vol. 210, no·. 3. Waorszawa.

M.I\CZ¥NSiKA S. ,1'9~8. ,Je·zo.wce ro'dziaoju DiS'coidea z cenoma.nu i turonu okoli-c K!l'a-

!lwwa, MiiechGwa i 'Wolbromia ~Cenomanian ,and TurGnian echlnoid'8 of genus Disco-idea fr'om the V'icdnity of Krak6w, lVLiech6w a,nod Wolbrom). - Pr-ace Muzeum 'Ziemi {Trav. du iMusee de la Terre),nr 2. ·Warszawa.

MULLER A. H. :'95(1. Weitere iBeHrage 7lUX I<lhnolog-ie, Straltinomie und Okologie del.' germani.schen Trias, Tetl

, r.

~ Geolo'gie, Jg. 5, H. 4/5. Berllin.

PAJNorw E . .1:9134. straltygrai,ia .k:.redy krakow.skiej (Sur la :S'tratdgraphie du Cretace des envdr·ons de Cm·co·vie). - Ro,ez. LP. T. Geol. (Ann. Soc. Geo!. Pol.), t. 10.

Krakow.

RADWANS!Kl1: A. 1·959. Struktury litoralne ^W ldas·ie w -Dolince Smytniej (Litto.ral structures (cliff, cla.stic di'kes and veins, and bor1ngs of. Potamilla) in the hi-gh-tatr'ic Li:as). - Acta Geol. Poll., v'ol. 9. Wars·zawa.

,191&5'a. Adddti-onal note,s on ilVIiio:cene Htto!l'al structures o.f Southern rp;oland. - Bun. A'cad. Pol. SeL, ser. ScL Geol. Ge.cgr., vol. il12, no. 12. Varsovie.

1,9:65b. Pr'Oce!!y wc!iskowe w osadach klastycznych i ·o'Olitowych (pitting processes in clastic and oolitic sediments). - Roc'Z.· P. T. Geol. (Ann. Soc.

Geol. lPol.), t. 35, z.2. KraU<::6w. .

11St67. Remarks 'On s'Ome Lower TOLrtoIllian br'OfWn-coal ibEaring sediments on the's'Outhern and easitern slopes od' the Holy Cross Mt:s. - Bull. Aead. Pol.

Sed.,

Ser.

Sci. <MDl., Geogr., 'vol. 15, InO. ,1. VarsoV1ie.

moo.

Tra'TI'sgresja doLnego tortonu na 'Obs·zarze Wyzyny Miecho'W,skiej d Kra- Ikowskiej (Lower 'Dortonian transg,res.sion onto the Miech6w and Cracow

Uplands). - Acta Geol. Pol., 'Vol. 1,8, .no. 2:. Warszawa.

1:2-Irr9. Transg.res.ja doineg·o :tortonu na poludniowych stokach

GDr

SwiE:tokirzys- kich·- sltreofa zatok 1 ioh przedpola (Lower Tortonian tr-ans,gre'Ss·ion onto the wuthe!l'lIl slopes of the Holy Cross' !Mts). ---:. Ibidem, V'GI. lⁱ9, 'Uo .. '1,

1il'7^IO. Dependence of xock;,.lborers and bUlI'towerson the ~vironmental

LOWER CENOMANIAN TRACE FOSSILS

conditions within the Toroonian Httoml zone of Southern Ip'oland. In: Crimes T. P. & Harper J. C. (,Ed.) , Trace fossdls. - Geol. J. (Spec. :Issu:e" no. 3).

'Liverpool.

RO:Nl'EWICZ P. 119'66. NeW data, .on sedimentation of Eocene organodetrital J.dmestones lin' the. Ta1lra Mts. - Buil. Aead. iPoIl.. Sm:,

sel'.

Sei. Gem. Geogr., vol. 11.4, no. 3. VlarlS'Ov~e.

'11970. BorlnglS and 'bU'n'OW1S dn the Eocene littoral deposd1;s 'of the Tatra Q\lIIOUl].taIials, tBoJand.

In:

,Orimes T. lP. & Harper J. C. (Ed.), Trace fos>511s. - ' Geol. J. (Spec. iIl'lsue-, n.o. ,3). Liverpool.

STEPHEN'SCN L. W.l'9512. ,ILarg€r dDlvelrtebralte fossils <Xf the Woodbine formation I(CenClllIlanian) of TeX'alS. - U. S. Geol.

:surv.

IPIrof. !Paper 24!2. Washiington.

TROGER K. A: 1969. iZur lPaJ.iionllologie, Biostratigra:pnie ,und f,aziellen Au:sbdldung del' u1llteren Obe1'kreide I(Cenoman 'bis ,':1"u1'on), Teil ilII. - Abh. Staatl. Mus.

Miine!r. Ge-ol., Bd. 113. Dresden.

VO]GT E. 1i970. Foram'iniferen und (?}phoronidea als Kommensalen auf den Hartgriinden del' Maa.siWi:cIMer Turftflaeide. - Paliiont.· iZ., Bd. 44, H. 1/2.

Stuttgart.

WRillGHT C. W. & WRIiGlHT E. V. 'lOOih A SlWV€Y of the fossill. lCe>phalo>poda of the Chalk 'Of Great Sri-tam. - ,Ba[aoontogr. Soc. (Monogr., vol. 104, no. 3. London.

ZAR~ZNY S. 1~8. 0 Sredndich waxst'Wiach Ikredowych w krakawsltim okr~gu. - Spraw. KolIll'is. affizjogr. Akad. Um., t . .1/2. lKu::ak6w.

- 10894. Atlas geologie:zny GaJ.1cyd (telmt do ze:szY'tu tr~iego). Kra!k6w .

•

J. GLAIZJEIK, R. MAROllNOiWSKiI J ll\. W~'KJl!

SP.!>STRZEZENIA NAD SIKAI.OTOCZAMI, STRATYGRAFIi\ I SEDYMENTACJi\

TRANSGRESYWNEGO CENOMANU W OKOLICACH KRAKOWA

(Streszczenie)

W czas-ie badan stratygraficznY'Ch i paleogeograficznY'Ch mezorotku w 8trefie lWyzyn srodkoWlopolskIch auto!rZY zaintE!r€s,oWlali is!i~ tr,ansgl'lesywnymi utworami cenomanu w kilku IOdsloni~ciach w okolicach Krakowa (fig. 'IB).Szcz€g6lnll uwag~

zwr6cnno na cha!l'aklter powierz.chru a!birazyjnych, rw kt6rych stwierdzono po !l'az pierws'zy liC'Zlle wydrllzen'ia skalatoczy (fig. le-E, ~3 oraz plo 1-2).

Na' podis'tawie dotychcxas cyitowanej Z Icenomanu krak,owSlkieg,a fauny (Za-

l'~czny l'1J7i8, 11894; 'iP'anow 1'9134; MllczyI1&k'a 1191518) if mnac'zenia przez IR. Mai'c-inowsk,ie- go amcmdt6w z Iwano.wIiIc: SchZoenbachia cf. varians {Sow.), S. subvarians Spath, S. subtubercuZata (Shal'\pe) d S. ventriosa Stiel., al\1iurzy wskaza/li, ze IW rejonie KXakowa udowodn'iony ifuunistyczme jest wylllcmie cenoman dolny (p1'zyjmujllc dwudzdeiny podmal Itego pi~a 8toslOWlany obecnde w P<llsce - por.Cieslinsiki 19S9, 11965; Matrcinow.slkd 1'970).

!Z powierzchni abrazyj'nych wieku dolnocenomanskiego opis'ano wydrllzenia gllibek 'CEntobia Bronn, 1'837, emend; Br:omley, 11I9'l10), wielosZ<!zet6w (,)pota.miZla

448 .TERZY Gl.AZEK, RYSZARD MARCINOWSKI & ANDRZE.T WIERZBOWSKI

Malmgren, 1'867", J>seudopolydOT'ites radwans"ii ichnogen. et ichnosp. nov.), mali6w (Myopholas Douvi1le, 1007) i jewwcaw. IWSlkamno, ze fo,rmy opisane przez S. Za-

r~nego{1'87'8) ,pod nazw~ "Scyphia sudolica" i uwazane za g~!bki s~ wistocie po-

~ostawionymi przez organizmy il'yj~ce ikanalami typu ThalasS'i7ioides Ehren'berg, 1944,

rozwini~tymi na I5cinanych abrazyjnie w dolnym cen{)manie mi~ich marglach g6ll'n{)jruraj.sk.ich.

W ,nawi~zandu do !paleoge'ogq'a~1i. gornej k.redy w rejonie kra:kowskdm roz- . pailrZlOno do'kmdndej charakter traIlBgresji cenomanskiej na ttyro obsmrze.

Instytut Gedlogii Podstawowej Uniwersytetu War8zawskiego Warszawa 22, Al. Zwirki i Wigury 93

WaTS'zawa, w marcu 1971 r.