Upper Visean conodonts from Orlej in the Cracow Upland: stratigraphical and paleothermal implications

Vol.

32.

ZDZIiSLAW BELKA

acta

gaOloglca polonica Warazawa 1982

Upper Visean conodonts from Orlej in the Cracow Upland: stratigraphical and paleothermal

implications

ABSTRACT: '1'he conodant fauna from the Upper Vmean deposits of the Cracow Upland, contacted by the subvolcamc P<)I1PhYJryinwuSiiJon,and ex,posed at the Orlej Qual'lry lincludes stIraJtigraphically .dmpo;rrbanJt forms, <iJllidicative of the Gnathodus girtYi colZinsoni Zone. The OOIliOdont-bearing algaJ.-foram.ind:fe:ral boundstones in theilr pOSltdeJpositiOll1al hlstory uIlider!werlit ,the therma:l \influence of the POIl"Phyll'lic initrusLon of Zalas. The employment .of conoclont alteraillion dndex (CAI) tindiJcaltes that the layer of algal-fo:ra:rmni!eral boulIldstones QCC,Ul1l'.ing 80 m off the con1laci with mtruSlion was 'heated {l·ver atemperatu.re of 210⁰ C during the pe;riodnot

shorter ,than 800 yearrs.

INTRODUCTION

The. Visean conodont faunas have been reported only from a few places in . Poland (see Skoropski & Sob0I1-Podg6rska 1980). These frag- mentary investigations do not allow to propose the conodont zonal sche- me for the Visean sequences 'of Polond. The majority ·of biostratigraphic data of the Visean "based on conodonts come from the Cracow Upland, southern Poland' (Gromc:mkiewic~-Lomnick~ 1974, 1979; Matyja & Nar- kiewicz 1979), precisely from several outcrops of the Carboniferous limestones in· the area north of Krzeszowice and of the investigated area of Orlej (cf. Text-fig. 1).

This study describes the conodont fauna from the Upper Vis€an sequence contacted by a subvolcanic intrusion of the Zalas porphyry, and exposed at the OrIej Quarry in the southern Cracow Upland (Text- -figs 1-2),being famous for a well preserved and very rich macro- fauna ' (cf. Czarniecki 1955). The conodonts from this very sequence were taken for the biostratigraphical and paleothermal studies.

Since many years, the cOil1odonts are us.ed for the biostratigraphy of Paleozoic and Triassic rocks. Recently; the cO,nodonts have also been used for determination' of the degree of heating of ·the rocks. (Epstein

58 Z. BEl..K.A

& al.1977, Bergstrom 1980). This method is founded upon the tempera- ture-induced color aiteration of conodonts, recognized by Epstein ^& aZ.

(1977), who leading the laboratory experiments and field observations demonstrated that the color alteration of conodonts is time and tempe- rature dependent (cf. Text-fig, 4), and thus it is directly related to the depth and duration of burial, and to the geothermal gradient. The color intervals distinguished by these authors were termed as color :alter-

KRZESZOWICE . GRAB EN

~6

Ds

Im?{'~/:I 4

..

.2

b;:-;·;·;·11

o , ^2km ,

Fig. I. GeoLogical map of· the. area oouth Qf Krzeszowice !in the Cracow Upland, w-ith !location IOf the Upper Vdsean sequence exposed at the Oriej Qwlir.ry . 1 PerrDian (velcMlic rocks, the· Zalas porphyry including), ,. Upper v~, 3 Namurian IIiIl.d Westphalian, 4 Juraaric, :; Miocene, 11 faults

a~ion indexes (CAI). The index values correspond to progressive ,and irreversible color changes from pale yellow (CAI = 1) through black (C~I = 5) to crystal clear (CAI = 8). This method is particular useful for. assessing organic metamorphism, because it is more rapid and inex- perisive than other organic maturity indexes,. Moreover, the color. alter- ation ofconod6n.ts provide thermal cutoffs for oil and gas and it allows to recognize the thermal history in areas of ancient igneous activity (Epstein &aZ. 1977) .

. Ac~nowledgements. The Author .. jjs. grClltefulto Profesaor A,Radwanskli for Cl'jticaJ. review .of the manuscript aIIlid several heLpful suggestiOlnlS, to Or. J ... An!!i.- lewskii and Dr. A.Kozlcitw\s.kIi for ,dlis,cw;SdJoo.,and S. Skompsk.i. for his help tin robe

~ield work.

UPPER VDSEAN: CONlODONTS 59

GEOLOGICAL SETTING

Near the village Zalas,in the southern Cracow Upland, there appears the' porphyric intrusion covered by transgressive Jurassic deposits (Text-fig. 1). According to Dzulynski (1955), the porphyries, about 100 m in thickness, sticking amid the Carboniferous rocks aresubvolcanic intrusion of a laccolithic type. The age of the intrusion has hitherto not been precisely determined. Siedlecki (1954) supposed that the ori- gin of the Zalas intrusion was connected with the Asturian phase (Stephanian) or with the Saalian phase (Permian), similary to what is the Variscan. age of the majority of intrusive rocks in the Cracow Up- land.

In the Orlej Quarry, the Zalas porphyries contacted with a sequence of black shales, over 100 m in thickness (Text-figs 1-2); the outcrop was described in detail by Dzulyitski (1955) and Pilat (1957). In the contact aureole, which is about 40 m thick, there occur shales showing thermal changes indicated by intensive silification. Among the black unmetamorphosed shales, to continue the section, there occur two .limes- tone layers (5 in Text-fig. 2). The shales which under- and overlie the limestones are richly fossilliferous. Thousands specimens of more than hundred species of macrofauna have been collected, mainly gastropods, pelecypods,trilobites, corals, bryozoans, blastoids,nautiloids, and bra- chiopods indicative of the uppermost Visean (Czarniecki 1955, 1956;

Gromczakiewicz-Lomnicka 1972). In the majority of cases the macro- :fossils were very well preserved. Unfortunately, the fossilliferous sha- les are not accessible at the present time. The limestones, to the con- trary, are very poor in macrofaunal remains, being representative of a plant-dominated community. These are strongly bituminuo\ls algal-

"':foraminiferal boundstones. The most important rock constituents' are a few centimeters higll moun.ds. built by the red alga Archaeolithophy~

NE

sw

o 20';'

:""-.,..;.-.~'

Fig. 2. Geological section showing the Upper Visean deposits contacted by the parphY\I'dic in1:lr·\liSI101n .in the Orlej Qualiry (after: Dzulytiski,1955; simplified) 1 Zalas porhyry, Z sandstonel!, 3 sil.1Cified shales (thermally metamQl'phoaed),4 oargillaceous males (unmetamor,phOlled), sa, ^b aIgal-fdraniiniferal . boundatoIlell (the ' coin,odont~bewing layer: i.s arroWed)

60 z. ^BEl.KA

Hum, encrusting foraminifer AphraZysia, and tubiform bluegreen algae referred to as GirvaneZZa by Belka (1981). Formerly, these structures were interpreted. incorectly as stromatoporoids .(Czarniecki 1955, 1956;

Dzulzynski 1955). The Orlej sequence represents the only outcrop. of the Culm facies to be supported bypaleontological evidence on the east fringe of the Upper Silesian Coal Basin.

Analogical facies to that occurring in the Orlej Quarry is widely extended in the Upper Pennsylvanian of North America, where the sets ("mounds") of phylloid algal limestones are developed· in much bigger proportion (Heckel & Cocke 1969). These carbonate bodies domi- nated by such leaflike or phylloid algae as ArchaeoZithophyZlum indi~

cate shallow-water marine conditions (Wray 1964; Heckel & Cbcke 1969; Toomey 1976, 1979), featured probably by limited water circula- tionandrelativly high rate of deposition. The sediments surrounding the phylloid algal mounds, mainly shales or calcilutitic limestones, are more open-marine. According to Heckel & Cocke (1969), these sedi- merits were deposited more slowly in slightly deeper water, where greater water circulation provided nutrients for more diverse and wides- pread biota. Phylloid algal-mound complexes of the Upper Pennsylva- nian occur between the open...:matine limestone facies and the terrigenous clastic facies. Their location in the upper part bf limestone units is interpreted by Fischer (1961) as a regresive feature of carbonate sedi.., mentation.

CONODONTFAUNA AND STRATIGRAlPHY

The conodont were collected from the algal-foraminiferal boundSto- nes occurring 80 m · off the porphyric intrusion in the Orlej QuarrY (layer 5a in Text-fig.· 2). A four-kilogram sample was procesed · for conodonts, and the following forms were recovered:

Gnathodus girtyi girtyi Hass

Gn. girtyi coZlinsoni Rhodes, Austin & Druce Gn. girtyi meischneri Austin & Humi

. Gn. girtyi rhodes.i Hig~ins HindeodeZla ibergensis BilScbOff HindeodelZa Sp..

Ligonodina Zevis Branson & Mehl Ligonodinasp.

Neoprioniodus peracutus (Hinde) Ozarkodina cf. pZana (Huddle)

Paragnathodus commutatus (Bmnson & MeW}

;E'. mononodosus(R,nodes, Austin & Druce) P. nodosus (Bischoff)

Number of specimens 7 1 1 1 3 6 1 2 1 1 2

~. 2·

ACTA GEOLOGICA POLONICA, VOL. 32 Z. BELKA, PLo 1

1 - Gnathodus girtyi meischneri !Austin & Husri; X 115

2- 7 - 6 Gnathodus girtyi girtyi - X 90, 7 - X 65 Hass; 2 - X 80, 3 - X 80, 4 - X 40, 5 - X 11~, 8-9 - Paragnathodus nodosus (BischoU); 8 - X 85, 9 - X 90

10 - Paragnathodus mononodosus (Rhoaes, Austin & Druce); X 100 11 - Paragnathodus commutatus (BranSon & Mehl); X 100

ACTA GEOLOGICA POLONICA, VOL. 32 ·Z. BELKA, PLo 2

1. - Gnathodus girtyi coHinsoni Rhodes, Austin & Druce; X 95; 2 - Gnathodus girtyi rhodesi Higgins; X 90; 3 - Gnathodus girtyi girtyi Hass; X 60; 4 - Gnatho- dus girtyi meischneri Austin & Husri;·· X 105; 5 - Ligonodina ? sp.; X 40; 6 - Ligonodina ~e1)is Branson &. Mehl; X 80; 7 - Gnnthodus girtyi girtyi Hass; X 120;

8 - HindeodeLla ibergensis Bischoff; X 75; 9 - Neoprioniodus peraclltus (Hinde);

X 70; 10 - HindeodeLla sp.; X 70; 11 - Ozarkodina cf. pLana (Huddle); X 80

UPPER VISE!\N CONODONTS 61

'I'he majority of the obtained forms · are characteristic of the Upper Visean/Early Namurian time. However, only two of the subspecies are sufficiently restricted in their ranges to be important for precise corre- lation. These are Gnathodus girtyi collinsoni and Gnathodus girtyi rho- d/i!si which indicate that Orlej fauna represents the Gnathodus girtyi coZZinsoniZone (sensu Higgins'1975). This zone was proposed by Rho-

des, Austin & Druce (1969) to include the upper part of the DsZone in the Lower Carboniferous of England (cf. Text-fig. 3), and its lower limit was taken at the first appearance of Gn. girtyi coZlinsoni. The upper limit of the zone has not been defined at that time. The subspecies Gnathodus girtyi collinsoni Rhodes, Austin & Druce occurs primarily in the uppermost ,Visean (cf. Gromczakiewicz-t.omnicka 1974, Higgins 1975, Skompski & Sobon-Podgorska 1980, Tynan ,1980), but in Ireland it has been recorded from the Pendleian (El) stage (Aldridge, Austin &

Husri 1968; Austin & Husri 1974). Therefore, Higgins (1975) restricted the stratigraphic range of Gn. girtyi collinsoni Zone to have its. upper limit marked by the first appearance of Gnathodus girtyi simplex;

this limit being simultaneously coincident with the Visean/Namul"ian boundary (ef. Text-fig. 3).

The second subspecies, Gnathodus girtyi. rhodesi Higgins has hit- herto been noted only from the uppermost Visean' deposits (Riggins &

Bouckaert 1968, Higgins 1975; Ramsbottom, Higgins & Owens 1969), so

flodo8UD

an. ~iUn.'3.atus bitiTUlatus Gn.. bi tinsa{;us

s u b d i v i s i o n s

England ( Higgin. 1975) eft,. biZineatus

England

Fig; :3. COIl"!relatlion of cOIIliOdont s'UJbdiv'~siOOiS and ffialC'rofawial ^'ZI0n6S of late Vi- seanJearly NamuTlian a~ !in western. EUil"rQPe

62 ^{Z. BEbKA}

it co-occurs with Gn. giTtyi collinsoni within the Gnathodus girtyi collinsoni Zone (sensu Riggins 1975).

In other regions of . Europe, the uppermost conodont zone of the Visean is based on the occurrence of Paragnathodus nodusus ⁽⁼ Gnat- hodus nodosus, = Gnathodus commutatus nodosus) which commonly occurs with Gn. girtyi collinsoni. This zone in Spam and Portugal em- braces the range of index species (Riggins 1974), but in Belgium (Ri- ggins & Bouckaert 1968), West Germany (Meischner 1970), Austria (Ebner 1977), and in the Pyrenees (Buchroithner 1979) it is a partial range zone, the upper limit of which is placed by authors differently, at the first appearance of the, index species diagnostic for the loca- lly accepted conodont zone. Similary to that, the position of the lower limit of ParagrUithodus nodosus Zone in particular countries is dia- chronous (cf. Text-fig. 3). The Paragnathodus nodosus Zone in West Germany has its lower limit in the middle of G0f3 (Meischner 1970) for instance, but in Belgium it already starts in Goo (cf. Conil & al.

197¹6). Nevertheless it seems, that differences in location of the lower limit of P. nodosusZone result rather' from the errors in correlation of particular conodont SUbdivisions with standard goniatite zonation than they are conditioned by natural facies or evolutionary factors.

Different location of the. lower and upper limits' of the Paragnathodus nodosus Zone cause that Gnathodus giTtyi collinso'tl-i Zone (sensu Rig- gins 1975) established in the Pennines, corresponds either to the upper part of the P .. nodosus Zone or, in other cases, to another part of that zone (cf. Text-fig. 3).

The fauna with Gn. girtyi collinsoni has also been described from North America; it occurs in the lower part of the Upper Zone A (Ty- pan 1980) correlated to the uppermost Visean, that is identicly as in. England.

Czarniecki (1955, 1956), basing mostly on the brachiopod fauna, determined the sequence of Orh~j as the uppermost Visean, correspon- ding to the Dr-Ds Zones of coral/brachiopod zonation in England. The recovered conodont fauna aliows to precise the age solely to the upper part of the Da Zone, being an equivalent to the Gnathodus girtyi collin;..

soni Zone (ej. Tex~-fig. 3).·

Consequently,' it .' is concluded that the Orlej sequence displays the sam~ age as the Ca'rboniferous Limestone deposits' cropping out to the SE of the quarry, "Nad Mlyn6wkq",. north of the Krzeszowice graben (Gromczakiewicz-Iiomnicka 1974), It represents the transitiomu shallow;,.

"'water facies· which was located between the 'terrigenous clastic facies and the. open marine carbonates. The other outcrops of the Lower Car- boniferous deposits In the Cracow Upland yield the conodont faunas Indicat~ve of the, Tournaisian and the Lower. to Middle Visean, i. a.

they are eVidently older (Gromciakiewicz.-t.omnicka 1974,'1979).

UPPER VISEAN CONTODONTS 63

P ALEOTHERMAL ANALYSIS

The conodonts from Orlej are generally black in color. With referen- ce to the color alteration index, the conodonts have the CAI value betw'een 4.5 and 5. Their color is due to thermal influence of the Zalas intrusion to the uppermost Visean rocks, and not due to their burial because the Carboniferous and Devonian conodonts known from seve- ral outcrops north of the Krzeszowice graben, have the CAI indexes not higher than 2. Nothing is indicated as well that at any time the thickness of the post-Visean deposits in the Zalas area was distinctly greater than that of the deposits north of the Krzeszowice graben.

The extreme temperature and time values of thermal influence of thesubvolcanic intrusion to the conodont-bearing layer were determi-

------- -----mal\----

---min--

w ~ CAI=1 I-

RE:CIPROCALOF ABSOLUTE TEMPERATURE

1°c ,.

Fig; 4.Almrenius plato! oonodant color alteration prepa:t1e.d by ~ &al.

(1977) on the laboratory experiments of conodont heating in open-air; diagonal lines indicate the CiolOtr alJterartrl.oo index (CAi); colOll" ~nteTVlal1s based on MU<Ilse'il soil wlar chiiPs; at CAI. = 4. to CAI. = .15 lConodont oolor lis blaak .

The field of 0010!l" alt.erartian for the Orlej oonodonts, ,is stippled; the usage of thiisplOll; fur detamniJnation ,cd anindmum and 'ma:x.imrum temperatures Illtlid time ranges (shq4ed tru;mgZe) fOr :t'he Upper Visean conodont6 from Qr.lej is e:x.pla,Loed

m the text· .

64 Z; BEl.KA

ned, based on the plot of color alteration indexes (Text-fig. 4) prepared by Epstein & aZ. (1977). ^It is possible to enumerate the maximum possi- ble time of the thermal activity of the intrusion basing on the geologi- cal data. The intrusion sticks amid the Upper Visean and Namurian rocks. Its Carboniferous cover at the roof was removed before the Jurassic, so the maximum possible time of thermal influence of the intrusion was not longer than about 110 m. y., the period between the Namurian and the Jurassic. The line of 110 m. y. yields to the 31 axis the maximum temperature value of 325° C. It is true, that for the field of CAl = 4.5-5 much higher temperatures are possible, for all it seems that the algal-foraminiferal boundstones have never heated over the temperature of about 300°C. The following facts advocate that:

(i) There ti;s :no eV'idence of ihe epigenef;ic ohanges evoked by 00IlItacl metamoc- phi,sm ,in this Jayer-. Sedimentary features, mLcrofaUJn.a and calcareous algae al"e exceptiO'lllally well preserved, and ,therefoce theoolonies of AphTolysia have reta- ined ~nal wall miof.Ostruoture, which allowed to recogndze ,their fomm·iruiferal nature (BeUm 1981).

(U) In the OOOlodont-beartiJIlg layer caloite is the most flrequenJt mineral (about SSO/e).

Moreover, these roclr.s oontain dolomite, and X-Tay anallysliB of .inSoOluble parts in

the

<

and a;patite. Amang these min.ea'als .there aJre no· assoc;iati,ons .specific of the facies of ,tlli:! we.adrest metamol1Phi.sm fOll'IIliiJngover the temperatwre 'Of 300° C (cf. TUil"Iler

& Verhoogen 1960).

(iii) .similar temperatwre data is shown by illiJte OCCUl'lfing in thea,}gal-foramini- feral bOUIlidstones. It d!s trequently u~ed to determine the degree of ;weak meta- mo.r.phism·The "mite CTystal1inity" has oommonly been. used as an evidence of metamwphic lrearysta1liZlaltion (cf. Dunoyer de Segonzac 1970). This ~ameter can be studied froOm the shape of time 001 peak: ,at 10 A. The illJitedetea:mIDatiOlIl in this study was maJde aClOOO'Iding ·to method of Gi1J.& at (1977). The m,iJte crys-talli- nity in the 'layer of al~al-Lomminiferal boutndstOlIl.es ShOWLS the value of 3.8 <indi- cative of the anchizone, which as the ,tra.nsition zone between ,the late.<liagenesis 8.l!l!d the epi:z'<me of r,e~onal metamorphism. 'Dhe anchiwne is p1aced about tem- perature of 2ilOo C. The above values correspond to the processes of the regional metamorphism, but we indirectly Clan use them beCause ,the d.!lite crystalllnd.ty is temperatur,e depedent f·irlst ·of all (DU:IlIOyer de Segonz,ac 1970).

The temperature of 325°C is very probable as the maximum possible temperature of heating of the conodont-bearing layer. Both lines of temperature and time maximum bound the triangle (Text-fig. 4); the corners of which mark the minimum values of temperature (210°C) and of the time (800 years). The real parameters of the thermal activity of the intrusion to the limestone layer correspond to the points lying within this triangle.

If the plot of Epstein & al. (1977) is correct for the longtime inter- vals, one may conclude that the conodont-bearing layer of algal-for"- aminiferal boundstones was heated over the temperature of 210°C, but

UPPER V1SEAN OONlODONTS

not higher than 300°C in the period between· 800 years and l1():m. y.

The . :real time of the thermal aCtivity' of the intrusion to the Iiiriestone larer is certainly related to minimum time value.

Institute of Geology of the Warsaw University,

At.. Zwirkii Wigury 93,

fJZ:"'089 Warszawa, Poland

REFERENCES

ALDRIDGE R. J., AUSTIN. R. L. & .HUSRI S. 196&. Vi~ oonodants from: North . W>ClIles and lireIa.nd. Nature, 219, 255-258. Lcmdon·

AUSTIN R. L. 1973. Modification .oflthe Brttish Av,O!ll~an conodoOrt7lonatioo. and a r.ea.m-aisal of EUJrOiPean D~ti.an oonodont -oonation and cOlTeiatiml. Ann.

Soc. Geot. ^BeZgique, 96 (3), 523-532. Blrus'se1s.

& HUSRI S. 1974. Dmnbiaal· COIliOdoInt faunas of Country Clare, Country,

Li~erick and Country Leitrim. An appendix. Int. Symp. Bela. Micropal.

Lim. "Namur 1974", 3, 18--64. Brussels.

BELKlA Z. 1981. The alleged algal genus AphraZysia isa forarn.inifer.N. lb. GeoZ . . PaZiionti Mh., 1981 (5), 257-266. .stutt~iI'I\:.

BERQSTROM S· M. 1980. CanodcIn.t 00101' altera1ljon as linrdicator of dncipientmeta- morphism \in OrdOrVlic~n. Il'ookls in SClallliddn~via' and the British Is1es. Abh.

Geol. Bundesanst., 35, 185~86. Vienna. . . .

BUCHROITHNERM, F. 1979. Die .con.adanJtenehronOll.~e i:m ~);)on der PY\f.e- '. nBeD.. Mitt. Osterr.Geol. Ges., 7Q, 75-1,18. VienIne..

CONILR.,GROESSENS

Eo

CZARNIlECKI S. 1956. :Lower. Cwrbooifenous fauna i:zl the Culm f~ r:4 ti)e eas- tem Upper Silesian. Coal

Baw.

1956. LOiwer OarbondferoUrs fauna Drom the Culm deposits of theeaawn part of U1e Upper Silesian . Coal Ba&iJn. ,[in Polish} Przeg1. Geoi., 1956 '(4), 177-178. Warszawa.

DUNOYER. de . ~EG(JNZAC G. 1979. The trainssfrorIllraltion of clay, mmerals d~~

diagent;sis and low~de rnetamqrphism: A reVliew. Sediment;oZogy, 15(3-4), 281--346. i\naste~~.

DZULYNSKJI S. 1955. .On th~ geologiml form of t~ porphYl'Y ;!in.the vi9ini.ty of·

Zalas (CracQW region) [in Polish]. Biul. ~.G., 97, 9~8.Warsiawa.

EBNER F. 1~'l7.~'Die pliederUIlg des ~rbon:s .von Graz mit Cqnodonten. Jahro.

peol. ^B.-:-A., 120 (2), 449-,400. Vj.erma..

EPSTEIN A. G., EPSTEIN J. B.&. ;HARRIS L. D. 1977~ ~t 00101l' a·lter- ation ....,... an .mdexto 0I'2a1Ilic metamarphism . . Geol. Surv. Prof· Paper,. 996.

1.:....27.

was;hiingtooi: .

FlSCHER A. G. 1961. Strn·ti·~phic recordo! It1raJnsl§ressing seas. in .light of sedi-

.mentation on Attantic coast of New Jersey. Amer .• Ass. Petrol. deal.. BuZZ.,

45, (IO),. d656--1666. 'Dulsa.

GILL W..D., KHALAF F· I. & MASSOUD M .. S. 1977. CLay IIP'l'lleI'<!lIS as an. dndex

of th~ 'de!§ree' of metamoz,phism of' ,the caIlbonat.e rand terrig6no~ ~~ks in

the South Wales ooalfield. Sedimfmtoiogy, 24 (4), 67lY...:...sin. Amsterdam.

GRIOMCZAKIEWICZ-LOMNICKA A 1972. Visean gastiropods from Orlej nea,r CraCOW~ Prace Muz. Ziemi, ZO, 3-44. Warsza'Wa.

s

61:1 Z. BEt.K.A

19'14., Upper, Va.sean riooodoot fauna,:from the ,CarboniferousL4mestone north )f. Krzeszowice, (environs of Cracow" Pqla~d). Ann. Soc. Geol. Pologne, U (4), 475-482. Kirak6w.

1979· Conodonrt; stratigraphy of the Uppermost Devoriian and Lower Carbo- niferous crockB in the Racla,w:kaand Szlclaxokta valleys west Oil Cracow. Acta GeoZ. Polon., 29 (4), 489-487. WaJr:Szawa.

HECKEL P. H. & ObCKiE J. M. 1969. Phylloli:d algal-mound com,plexes dn outc:ro- pping Upper Pennsylvanian crocks of Mid-Continent. Amer. Ass. ^Petrol.

Geol. Bun., 53 (5), 1058-1074. Tulsa.

HIGGINS ,A. ;1974. Conodont ronation .of the Lower Carbondferous ,of Spain and Portugal. Int. Symp. Belg. MicropO,l. Lim. "Namur 1974", 4, 1-.17. Brussels.

1975. Conodont zonaJbion of rthe late Vi:sean - early WestphaHalll strata of ,the south' and central Pennines of northern EDgland. Bull. GeoZ. Surv. Gr.

Brit., 53, 1-90. London.

&' 'BOtrCKAERT' J: 1968· C()I[).()dant stratigraphy and palaeontology .of the Nanl.ttni.an of Belgiurn. Mein;ExpZ. Cartes Geol. Min. Belgique, 10, 1-64.

Brussels.

MATYJA 'H.& NAaKIEWICZM. 19'19. Liitbofacies and conodonts IinVisean pro- tile, ,OLkWlZ acrea, southern. P.oland. Acta. Geol. Polon., 29 (4), 475-488. War- szawa.

MEISCHNER D; 1970. Conodonten-Ohronol6gie des deutschen Karbons. C.-R. 6^e Congr. Inter. Strat. GeoZ. Carbon.,· Sheffield 1967, 3, 1169-1180. Sheffield.

PILAT T; 1957. Pot'lphylrlc pebbles' from the shales of the Uptper Visean of the ll'egionOi Zalru; (Ccracow region) ,[in Polish]. Biul. 1. G., 115, 167-'-1194. War-

szatWa.

RAMSBOTTOMW. H. C·,HIGGINS A~ C. & 'OWENS B. 1979. Palaeoo,tologWal chaoraclerdisatoon of the Namllltian' .of the stra'totype aa.-ea (a report of the NamurianWorking Group); C.-R. 8^e Congr. Inter. Strat: Geot Carbon.;

Moscow 1975, 3, ~99.Moscow.

RHODESF. H. T., AUSTIN R. L. &' DRUCE E. C· 1969~ British :Avondan (Carbo- niferous) Cantodonits faunas andthe1cr vadue iD. local &lld' linta-continlental carreliation. Bun. British Museum (Nat. Hist.), Geology, SoW!. 5, 1-313.

London.

SIEDLECKI S. 1954~ .l:'aleozOlC Iormations of' the' Cracow region I[in Polish]. Bim.

1· G., 73, 1-415. War\SZalWa.

SKOMPSKI' S. &8C>BON-FODGORSKlA J,.' 1980. 'Farainimfers and conodoots in the Viseandli:!pOsdA;s Of ,the Lublin Upland. Acta Geot Polon., 30, «1), 87-416.

W8il"szarwa.

TOOMEY D. F~ 1976.,PaJeosyneoolcigy ofa Penman plooit dominated marine oonliriwDJi,ty. N.' Jb. Geol. 'PaUJ.ont. Abh~, 152 (i), 1--18. Stuttgart·

1979. ',' Role ',of archaieol1thqphyllfd illgae:within 'a lciteCa/dxmliferous aIgal- -sponge oommunity, southw.estern United States. Bull. Cent. Rech. ExploT.- -Prod. EH-AqUitaine, 3 (2), 84~53. Pau~

TURNER· J. T~ & VERHiOOGEN J. '1960. Igneous' and ffietamoIrphlcpekologyj 2nd ed. iNew Yocrk.

TYNlAN M, C. lUOO. Coinodont biOSltratigrtllphy of the MissiSsippian Chainman For-

~tion, !Western Miiliall'd Country, Utah. J. Paleont., 54 (6), 1282-'-1309. Tulsa.

WRAY J. L. 1964. Archaeolithophyllum, an abundant calcareous 'alga in limesto-

nes

the

Sur';. Bull·, 170 (il). '1-13. LMvil'ence~

UPPER VISEAN OONODONTS

67

z. ^BFLKA

GORNOWIZElQ"SKIE KONODONTY Z ORLEJA NA WYZYNIE KRAKOWSKIEJ JAKO WSKAZNIK STRATYGRAFICZNY I PALEOTERMICZNY

(Streszczenie)

W osada,ch g6mego wizenu kontakJtujllcych z .intruzjll porfk6iW zala.s.kdch

w 'kamieniolomie Orlej (Jlig. 1-2) stwrerdz<mo oboonosc konodom6w (par. pl 1~2).

Poz,waJajll one precy!zyjmej .okr"eslic 'Wd.ek tych osad6.w ocipowiadajllcy rzonie Gnat- hodus girtyi collinsoni w podziale Higginsa (1975), kt6ra s~a;nowli najwyzszll lrono- donWwIl ZOll1~ rwli.zenu (por. fig. 3).

Larwica wapieni algowych zaJWiie:rajqcych konodonty zos:tala pooddana te.rmicz- nemu oddzlialyrwamu intruzj,i zalasikiej, ()Q wywolalo rmnian~ balrwy konodont6w na ('1977), c.zmonq. ldt6ry Dm~ pokazuje zasrtosowaniu wykresu zmiany barw konodont6w w zalemoSci od czasu sk()ThSltrlllowane~ 'prrzm Epsteina i tempe-& at rntury (pOT. fig. 4), wykazano, ze lawica wapieni algowych z Orleja byla pod':' grzana powyzej 2l0oC (leez nie ponad 32S0C) przez. okres nde kr6tszy ndz 800 Lat.