V ol. X L V II — 1; 11—25 K r a k ó w 1977
Kazimierz
M a t l ,Teresa
Ś m ig ie ls k aPALAEOGENE MARINE SEDIMENTS BETWEEN GŁOGÓW AND SIEROSZOWICE
(LOWER SILESIA - POLAND)
(Pl. I—II and 2 Figs)
Morskie osady paleogenu między Głogowem a Sieroszowicami (Dolny Śląsk — Polska)
(Tabl. I—II i 2 fig.)
A b s t r a c t : On the basis of lithology and microfauna m arine sedim ents of Upper Eocene, Lower Oligocene and Upper Oligocene in the Głogów — Sieroszowice region ате stated. They are clastic sedim ents w ith intercalation o f limestones, sandy glauconitic lim estones and marls separated by erosional surface.
INTRODUCTION
The boreholes drilled during the last few years on th e F ore-Sude tic Monocline ( F r a n k i e w i c z , M a t l , 1975) south a n d south-w est of Gło
gów (Lower Silesia, Fig. 1) p en etrated an interesting section of beds of m arine origin in the low erm ost p a rt of the Cenozoic cover. The beds overlie d irectly the surface of the Mesozoic basem ent show ing a d iversi
fied relief, ch aracterized by a prevalence of m orphological form s strik in g NW-SE (ooncordantly w ith th e m ain tectonic dislocations of th e M iddle O dra zone).
The lithological type of the sedim ents, as w ell as ab u n d an t m acro- an d m icrofauna found in them , point to th eir m arine origin.
The m icrofauna was m entioned by O d r z y w o l s k a - B i e ń k o w a (1973), who based h e r investigations, on 4 sam ples derived from bore
holes in th e region of Sieroszowice. Sedim ents w ith sim ilar lithological features are assigned a t p resen t to th e Oligocene, to th e s.c. Lubusz Form ation ( D y j o r , 1970, 1974) an d correlated, p a rtly incorrectly, w ith various stra tig ra p h ie units of the Oligocene of Polish Low land estab
lished by С i u к (1970, 1974).
A thorough stu d y of m icrofauna related to the lithological features of the sedim ents encouraged the p resen t authors to suggest a new a p proach to the stratig rap h ie units in th e area in question. The m icrofau- nal assem blages rep resen t a profile com prising sedim ents from the U pper Eocene to the bottom of th e U pper Oligocene w ith stratig rap h ie hiatus in the M iddle Oligocene. Those sedim ents fill the g reatest depressions in the basem ent surface, the younger units usually overlapping the older ones. The relationships betw een the m orphology of the basem ent an d occurrence of sedim ents becomes o b literated only in the U pper Oligo
cene, the boundary of w hich is delim ited by lines of regional signifi
cance.
U pw ards, m arine sedim ents pass, for the m ost p a r t continously, into continental coal-bearing deposits of the upper p arts of the U pper O li
gocene.
The whole Palaeogene attain s in some localities (Jakubów, Jerzm a
nowa) a thickness of 96 m (Fig. 2) averaging 60 m. The thickness of m arine sedim ents am ounts to 54 m , being actu ally m uch sm aller since it does n o t generally exceed 30 m in individual profiles.
DESCRIPTION OF SEDIMENTS
U p p e r E o c e n e . The U pper Eocene sedim ents have th e sm allest extent. T hey fill the greatest depressions in the basem ent, form ing an isolated and elongated cover w hich extends over a n area of 15 k m 2, b e
tw een Bukwica in NW an d Jerzm anow a an d Bądzów in SE. The sedi
m ents re s t directly w ith a considerable stratig rap h ie hiatus on the in ten sely lithified, re d K euper sandstones.
The rem n an ts of th e U pper Eocene cover a re recorded 7— 8 km SW an d S of Głogów. They a re isolated an d in no d irect contact w ith sedi
m ents of sim ilar age, lying fa rth e r to the n o rth (e.g. in the region of Wschowa or Góra), thereby occupying the southernm ost position. This fact indicates th a t the U pper Eocene transgression in the W est P oland had a su b stan tially g reater e x ten t th an it has been assum ed so far.
U pper Eocene sedim ents have been found in six boreholes (Fig. 2) a t a depth of less th an 400 m; th eir thickness varies from 14 to 20 m.
T here is e ith e r a continuous sedim entary succession betw een the U pper Eocene a n d the Lower Oligocene, or an erosional surface, an d th en the U pper Eocene comes into direct contact w ith sedim ents of the m iddle p arts of th e U pper Oligocene. The U pper Eocene sedim ents are, as a rule, strongly calcareous, dark glauconitic sands and green, fine- an d m edium grained quartz-glauconitic sands. G lauconite forms num erous grey-green concentrations (up to 45%) in the quartz-glauconitic sand, which also contains fine concentrations of black phosphorites.
A ch aracteristic featu re of the profile from Bukwica (borehole S — 380) is the presence of glauconitic san d y m arls an d oolitic lim esto
nes w hich form six intercalations from 0.05 to 0.8 m in thickness in the upper p a rt of th e sand complex. In places, the sands pass into strongly calcareous glauconitic sandstones. The profile in question is eroded a t the top of the last, upperm ost lim estone intercalation, w hich implies th a t it is incom plete an d reduced.
In all types of the U pper Eocene sedim ents of the profile from B uk
wica, a b u n d an t a n d diversified m acro- an d m icrofauna has been found.
A complete profile of the upperm ost p arts of the U pper Eocene has been ascertained in boreholes in the region of Jerzm anow a an d Jakubów (S — 350 amid S — 365). SE of Buikwica, calcareous q u artz glauconitic sands w ith phosphorites and, occasionally w ith intercalations of sandy lim estones or calcareous sandstones have been noted. They pass conti
nuously into th e Lower Oligocene sandy glauconitic sedim ents. The U pper Eocene — Low er Oligocene boundary is m ark e d both by m icro- fa unal assem blages an d by th e lithological ch aracter of the sedim ents.
L o w e r O l i g o c e n e . T here is a continuous sedim entary succession betw een the U pper Eocene and the Low er Oligocene. The la tte r is r e presented exclusively by calcium -free fin e- an d m edium -grained quartz sands w ith a low glauconite content. T heir thickness in th e regions of Jakubów an d Jerzm anow a is 15 m an d 23 m, respectively.
The Low er Oligocene sands a re characterized by:
— a su b stan tial decrease in th e glauconite content,
— the lack of calcium a n d the absence of lim estone an d m arl intercala
tions or phosphorite concretions,
— disapperaence of num m ulites in the m icrofaunal assem blage and a su b stan tially higher co n ten t of planctonic foram inifera,
— a sm aller am o u n t of both m acro- an d m icrofauna.
The profile of the Lower Oligocene ends w ith an erosional surface th a t determ ines the contact w ith sedim ents of the m iddle p a rt of the U pper Oligocene. In none of th e boreholes the sedim ents of th e Eocene- -Low er Oligocene sea have been found to pass directly into Middle Oli
gocene continental deposits. It appears, therefore, th a t the em ergence of older sedim ents an d th eir erosion took place in th a t period. N evertheless, it seem s th a t th e presence of rem n an ts of the M iddle Oligocene conti
n en tal sedim ents in the area u n d e r exam ination is v ery probable.
U p p e r O l i g o c e n e . The profile of Palaeogene m arine deposits in the area betw een Głogów an d Sieroszowice is term in ated by a sedim entary complex rep resen tin g the low er p arts of th e U pper Oligocene. The U pper Oligocene sedim ents have been recorded in two boreholes (S-382 an d S-376), 9 km a p a rt, localized on th e n o rth e rn a n d eastern side of the Eocene cover n e a r Bukwica-Dankow ice an d K urów (Fig. 1). In one bore
hole they re s t d irectly on the Triassic basem ent, w hile in the o th er on continental deposits of indefinite age. The position of the la tte r under the U pper Oligocene m arine sedim ents m ay point indirectly to th eir Middle Oligocene age.
Fig. 1 — Localization of boreholes that penetrated the maxiine Palaeogene in the region of B ukw ica and Jerzmanowa. 1 — investigated area; 2 — localization of bore
holes
Fig. 1 — Szklić sytuacyjny otworów wiertniczych przebijających paleogen morski w rejonie Bukwdcy i Jerzmanowej
U pw ards, the m arine sedim ents pass, presum ably continuously, into continental sandy-m icaceous deposits and, higher up, into coal-bearing deposits of the m iddle and upper p a rt of the U pper Oligocene.
A t B ukwica-D ankow ice, the U pper Oligocene m arine deposits a tta in to a thickness of 8 m. They a re rep resen ted (Fig. 2) by clayey-calcareous sedim ents m ade up of m arly clays w ith glauconite an d 1— 2 beds of grey m arly lim estones (up to 0.4 m thick) w ith anim al burrow s. In both types of sedim ents nests an d dolls of p y rite have been noted.
In the upper p a rt of the profile th ere have been recorded grey m arly clays w ith a considerable sand content an d d ark -g rey argillaceous m u d stones w ith glauconite an d m acrofauna shells.
A facially d ifferen t sedim ents has been encountered n ear K urów.
They consists m ainly of quartz sands w ith a high mica (muscovite) con
te n t a n d tw o horizons of quartz-gjlauconitiic argillaceous sarnds, lying about 10 m ap art. A characteristic featu re of th a t profile is a su b stan tial concentration of w h ite mica flakes both in the quartz sands an d in the sands w ith glauconite.
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The U pper Oligocene m arine horizon is overlain by a th ick (up to 25 m) complex of continental quartz sands w ith w hite mica flakes and gravel pebbles (Fig. 2). The m arine ingression was short, its effects dis
ap p ear gradually tow ards the south-east.
THE CHARACTER AND DISTRIBUTION OF FAUNA
In all the m arin e sedim ents betw een Głogów and Sieroszowice, older an d younger Palaeogene m icrofauna have been found. Some sam ples contain rich a n d w ell-preserved m icrofaunal assem blages composed of benthonic, m ainly calcareous an d ra re ly agglutinating, foram inifers. Large foram inifers a re rep resen ted by num m ulites, fairly ab u n d a n t in some sam ples, and single operculines. In other sam ples a few planktonie fora
m inifers, globigerines have been found.
A p art from foram inifers, scarce radiolarians an d o th er protozoans in
cluded am ong T intinnida m ay be encountered, as w ell as m acrofauna rem ains, e.g. v ery ra re skeleton elem ents of sponges, corals, tubes of an nelids, bryozoans, brachiopods, pelecypods, gastropods, spines of echi- noids, ostracods, fish scales, teeth an d otoliths.
Typical foram iniferal m icrofauna ch aracteristic of th e U pper Eocene sedim ents, consisting of abundant, w ell-developed an d diversified forms, has been found in the low er p a rt of th e profile S-365 (at a depth of 497—498.8 m). In a sand-glauconitic sedim ent th e m icrofaunal assem bla
ge is rep resen ted (Pl. I) by num erous M iliolidae (Spiroloculina, Q uinque- loculina, Triloculina, Spirophtalm idium , Lacazinella), Polym orphinidae (Reusselia sp., Biapertorbis cf. brandenburgensis K iesel et Lotsch, Baggina iphigenia (Samoilova), Asterigerina rotula haeringensis L ü h r (abundant), Pararotalia lithotham nica (U h 1 i g) (abundant), Pararotalia inaermis (T e r q u e m), P . audouini (d’O r b i g n y), Cibicides carinatus (T e r - q u e m), Cibicidoides bellus M j a 1 1 u k). N um m ulites a re rep resen ted h ere by two species: N u m m u lites concinnus J a r c e v a an d N. orbignyi (G a 1 e о 1 1 i). M oreover, T intinnidae, num erous ostracods, m ainly thick- -shelled w ith sculpture, an d the m acrofauna rem ains, listed above, have been found in this p a r t of the profile.
Fig. 2 — Corrélation of the Palaeogene profiles in the area betw een Głogów and Sieroszowice. 1 — gravel; 2 — sand; 3 — silt; 4 — sandy clay; 5 — clay; 6 — lim estone or marl; 7 — coal clay; 8 — brown coal; 9 — borehole section without drill core; 10 — m uscovite concentration; 11 — microfaunal assem blage w ith nummulites;
12 — microfaunal assem blage with globigerines; 13 — microfaunal assem blage with Asterigerina gürichi gürichi; 14 — radiolarians; 15 — correlation lines; 16 — surfaces
of erosional discontinuity
Fig- 2 — Zestaw ienie korelacyjne profilów paleogenu w rejonie między Głogowem a Sieroszowicami- 1 — żwir; 2 —. piasek; 3 — mułek; 4 — ił zapiaszczony; 5 — ił;
6 — wapień lub m argiel; 7 — ił węglisty; 8 — w ęgiel brunatny; 9 — odcinek otworu pozbawiony rdzenia wiertniczego; 10 — koncentracja muskowitu; 11 — zespół mikro
fauny z numulitami; 12 — zespół mikrofauny z globigerinami; 13 — zespół mikrofauny z Asterigerina gürichi gürichi; 14 — radiolarie; 15 — lin ie korelacyjne; 16 — poziomy nieciągłości erozyjnych.
2 — R o c z n ik P T G X L V II/1
In th e h ig h er p a rt of th e profile m icrofauna becomes fin er (Pl. II. Fig.
1). A t a d ep th of 480— 483 m globigerines, re p re se n te d by, e.g., Globige- rina danvillensis Howe et W allace an d G. officinalis Subbatina, as w ell as by o th e r foraim nifers have b een found. T hey a re : S vra tkin a perlata ( A n d r e a e), Chilogümbelina gracillima ( A n d r e a e), Bolivina fastigia C u s h m a n , ß. tereta (C u s h m a n), Alabam ina w olterstorfii ( F r a n k e ) , sanie species of Cibicides an d re la te d genera, an d various species of Po- lym orphinidae. T h at assem blage m a y be reg ard ed as rep resen tativ e of the E oc en е/ OlLgoe ene boundary or of th e low er p a rt of th e Low er Oligocene (M a r k s a n d V e s s e m , 1971).
Since the logging has been incom plete and th ere are gaps in the up
per p a r t of the profile (at a depth of 460— 480 m), it is im possible to give its fu ll characterization on the basis of m icrofauna. In the higher beds (at a depth of 457— 460 m) organic fossils are missing, an d at a d e p th of 437— 442 m only flora rem ains have been found.
A n Eocene foram iniferal assem blage has been also recorded in the borehole S-380, from w hich 50 sam ples w ere investigated. It consists p artly of the species reported from the U pper Eocene sedim ents, e.g.
Pararotalia lithotham nica, Cibicides carinatus, b u t also some others, e.g.
Melonis ornatissim um ( C u s h m a n ) , Oolina sphaericostata ( G r z y b o w s k i ) have been noted there. However, Asterigerina rotula haeringen- sis, the species v ery common in th e borehole S-365, is missing altogether.
S m all foram iniferal m icrofauna is relativ ely scarce in this profile. On the other hand, it is interesting to note, th a t num m ulites a re ab u n d an t there. Thus, a t a d e p th of 420.25— 423.25 m, N u m m u lites ex gr. vario- larius ( L a m a r c k ) an d N. orbignyi, an d higher N. orbignyi (f. A and f. B) have been found. From 414.75 m upw ards, both N. orbignyi and N. concinnus are present. This sequence of num m ulites m ay indicate that, up to a depth of 410 m, the profile under stu d y represents a slig h tly older U pper Eocene sedim ent than th a t re p o rte d from the bore
hole S-365. This assum ption can be supported by th e presence of N u m m ulites ex gr. variolarius in th e low er p a r t of the profile S-380, whose species is know n to occur from th e M iddle L utetian to the M iddle B ar- tonian, resem bling N. paravariolarius J a r c e v a , The au th o r of the spe
cies assum es th a t it is an interm ediate lin k betw een N. variolarius and N. orbignyi, an d h e r opinion has been su p p o rted by the studies of the p resen t m aterial. M oreover, the sim ultaneous occurrence of a b u n d an t N. orbignyi w ith scarce N. concinnus m ay also evidence the faćt th a t the investigated p a r t of ifche pro file rep resen ts a som ew hat low er horizon of th e U pper Eocene.
N u m m u lites concinnus is reaching the highest p a rt of the U pper Eo
cene; it has been noted even in L atto rfian sedim ents ( J a r c e v a e t al., 1968). In th e discussed in terv al it did not attain , however, its m axim um developm ent in contradistinction to N. orbignyi, w hich appears in the
U pper L u tetian and does not go beyond the U pper Eocene boundary.
T hat species is a b u n d an t in the p resen t m aterial.
In the m aterial un d er exam ination no m icrofauna representing the Middle Oligocene — Rupelian, w hich corresponds to the G erm an S ep ta- ria-clay horizon, has been found. The characteristic species such as Ce- ratobulim ina contraria ( R e u s s ) or Rotaliatina bulimoides (Reuss) are ab sen t there (W o 1 a ń s к a, 1962; G o r t y ń s k a , 1962).
U pper Oligocene m icrofauna (Pl. II, Fig. 2) has been found in the borehole S-376. N um erous foram inifers of the species A sterigerina gürichi gürichi (F r a n k e), Angulogerina gracilis tenuistriata C u s h m. et E d w. : A. gracilis germanica C u s h m . et E d w., Sphaeroidina variabilis R e u s s , Cribrononion subnodosum ( R o e m e r), E lphidium hilterm anni H a g n, P rotelphidium roem eri ( C u s h m.), M elonis ajfine (Reuss) have been noted a t a depth of 404 m. The occurrence of the species Asterigerina gürichi gürichi is of p a rticu lar significance; it defines the s.c. „A sterige
rin a zone”, assigned by most of the W est-European investigators to the low er p a rt of the U pper Oligocene — the C hattian (B a t j e s , 1958; E l l e r m a n n , 1958; I n d a n s , 1958; K i e s e l , 1962). O th er accom panying species have also been rep o rted from younger Oligocene sedim ents of N orth G erm any, Belgium ( B a t j e s , 1958) and Poland, e.g. near Izbica K ujaw ska (P o ż a r y s к i, 1953).
The successive m icrofauna fossil rem ains occur higher up, only a t a d ep th of 393 m. They a re scarce radiolarians — Cenosphaera sp., Spon- giom ma sp. — w hich, according to Soviet au th o rs (S u b b o t i n a, P i- s h v a n o v a , I v a n o v a , 1960), a re characteristic of the Lower Mio
cene. A p art from them , sporadic globigerines, rem ains of pyritized fora- m inifers an d fragm ents of ostracods have been noted there.
The m icrofaunal assem blage found in only one sam ple from the b o re
hole S-382 is sim ilar to th a t noted in th e low er p a rt of the profile discussed above. It is rep resen ted by single specim ens of Nodosaria ewal- di R e u s s (fragm ents), L enticulina sp., some species of Polym orphinidae, single A sterigerina gürichi gürichi and Angulogerina sp., ab u n d an t Cibi- cides sulzensis ( H e r m a n n ) , scarce M elonis affine an d E lphidium h il
term anni, a n d m acrofauna rem ains: tubes of annelids, pelecypods, gastro
pods, spines of echinoids an d fish rem ains. The above assem blage is poor
er both in q u ality a n d q u an tity an d less characteristic th a n th a t found in the borehole S-376. It rep resen ts presum ably a som ew hat low er s tr a tigraphie horizon, m aybe a t the boundary of the R upelian an d C hattian, w hich is evidenced by th e scarcity of Asterigerina gürichi gürichi an d the abundance of Cibicides sulzensis. It seem s th a t this p a rt of the pro
file m ay be co rrelated w ith th e s.c. Boom clay sedim ents extending throughout NW Europe an d being a u n it of tihe Oligocene a t the bound
a ry of the R upelian a n d C hattian.
CONCLUSIONS
A n early com plete profile of Palaeogene sedim ents of W est P oland is preserved in the area betw een Głogów an d Sieroszowice. I t com prises sedim ents from the U pper Eocene up to the bottom of the Miocene, w hich re s t directly on the Triassic basem ent. All the fu n d am en tal stratig rap h ie units m ade up of m arine sedim ents are fu lly docum ented by m icrofauna.
Their palaeontological distinctness has been also confirm ed by lithologi
cal ch aracter of the sedim ents.
Due to th e index m icrofaunal assem blages, two m arin e ingressions have been identified in the studied profile: older, having occurred in the U pper Eocene an d the Lower Oligocene, and younger in the U pper O li
gocene.
The U pper Eocene ingression took place during a som ew hat extended period of time. Its beginning m ay date back to the m iddle p a rt of the U pper Eocene (Middle B artonian — region of Bukwica, th e borehole S-380), w hich is docum ented by the abundance of N u m m u lites ex gr. va
riolarius know n from th e Lower L u tetian to the M iddle B artonian. This species disappears in the up p er p a rt of the B artonian in the region in question a n d is also missing in o th er boreholes investigated so far (S-350 an d S-365). The basin changed its ch a ra c te r a t the tu rn of th e Eocene an d Low er Oligocene (disappearance of num m ulites, evolution of litho
logical featu res of the sedim ent), b u t m arine sedim entation w ent on u nin
terru p ted . F u rth erm o re, this is one of the few localities in P oland w here it was possible to dem onstrate th e continuity of the profile a t the Eoce- ne/O ligocene boundary ( O d r z y w o l s k a - B i e ń k o w a , 1966).
The sedim entation w as in te rru p te d only a fte r the Low er Oligocene (or during its culm ination), th e discontinuity com prising presum ably a con
siderable p a rt of the M iddle Oligocene (Rupelian) and, in some profiles, also low er p arts of th e U pper Oligocene (Chattian). In th e whole a re a in question th ere is no typical equivalent of the Middle Oligocene sedim ents w ith distinctive phytogenic accum ulation, an d n eith er is this u n it docu
m ented by m icrofauna. M oreover, U pper a n d Lower Oligocene m arine sedim ents a re m issing in several places.
The successive, younger m arine ingression occurred in the low er p a rt of the U pper Oligocene. I t has a substan tially g reater regional extent, covering th e area occupied by the U pper Eocene and Lower Oligocene sedim ents. F auna has been found in the profiles of the NW p a rt of the region (Bukwica, Dankowice, Kurów). A characteristic featu re of the U p
per Oligocene sea is a m icrofaunal assem blage w ith the index species A sterigerina gürichi gürichi an d single radiolarians. Towards SE (SE of Jerzm anow a), m arin e sands w ith glauconite form thin intercalations (0.4— 1.0 m) in the brackish and, presum ably, also continental q u artz sands. M icrofauna gradually disappears in the sam e direction.
The U pper Eocene m icrofauna found in the investigated sam ples is clearly of a shallo w -w ater character, w hich is evidenced by a high con
te n t of foram inifers from fam ilies Miliolidae, Polym orphinidae, R otali- idae, N um m ulitidae, an d the subfam ily Cibicidinae. It is the fauna th a t some G erm an a u th o rs have defined as fauna of the ’’C alau” type (K i e- s e l , L o t s c h , 1963; K i e s e l , 1970), i.e. shallow -w ater, therm ophilous,
found in seas of norm al salinity.
S im ilar conclusions em erge from th e stu d y of m acrofauna, w hich is represented by, e.g. annelids, bryozoans, rem ains of echinoderm s, ostra- cods, usually thick-shelled w ith sculpture, living in littoral, w ell aerated w aters, an d T intinnida from protozoans. The la tte r have been also r e ported from th e U pper Eocene sedim ents, in w hich some of them occur in sand-glauconitic m arly clays, in assem blages containing foram inifers, molluscs, fragm ents of echinoderm s, i.e. sim ilar to the assem blage in question. T intinnida found in the T ertiary sedim ents, p articu larly those rep o rted from the Eocene, a re included am ong organism s living in re la tively shallow w aters of norm al salinity. The presence of num m ullites, w hich are freq u en tly very abundant, as w ell as the prevalence of cal
careous form s am ong the foram inifers im ply th a t the sea w a te r was rich in Ca ions.
The Palaeogene profile in the region betw een Głogów an d Sieroszo- wice m ay be co rrelated w ith the lith o stratig rap h ic division of С i u к (1970, 1974) a n d D у j o r (1974), as it is show n in Table 1.
The specific lithological type of the U pper Eocene sedim ents in the region of Głogów gives grounds for the distinction of th e Sieroszowice Beds as a sep arate lithostratigraphic horizon. M icrofaunal studies also ju stify the tra n sfe r of the Jerzm anow a Beds of D y j o r (1974) to the U pper Oligocene.
A cadem y of Mining and Metallurgy, Institute of Geology and Mineral Resources Al. Mickiewicza 30, 30-059 K raków
K azim ierz Matl ■— D epartment of Brown Coal Deposits
Teresa Śmigielska — D epartment of Palaeontology and Stratigraphy
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C i u k E. (1970), Schem aty litostratygraficzne trzeciorzędu Niżu Polskiego (Litho- stratigraphical Schem es -of the Tertiary from the Polish Lowland Area). Kwart, g eol, 14, 4, pp. 754—771, Warszawa.
С i u к E. (1974), Schem aty litostratygraficzne paleogenu Polski poza Karpatami i za
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E l e x m a o n C. (1958), Die m ikrofaunistische Gliederung des Oligozäns im Schacht Kapellen bei Moers (Niederrhein). Fortschr. Geol. Rheinl, u. Westj. 1, pp.
205—214, pis. 3, Krefeld.
F r a n k i e w i c z J., M a t l K. (1975), Podział i w ykształcenie trzeciorzędowej form a
cji węglonośnej w rejonie Lubin — Głogów. Arch. Inst. Geol. i Sur. Mineral., AGH, Kraków.
G o r t y ń s k a S. (1962), Kilka uwag o oligocenie w Polsce .zachodniej (Some re
marks on the Oligocene of W estern Poland). K w a rt, geol., 6, 1. pp. 125—133, Warszawa.
I n d a n s J. (1958), Mikrofaunistische Korrelationen im m arinen Tertiär der N ie- derrheinischön Bucht. Fortschr. Geol. Rheinld. u. Westf., 1, pp. 223—238, pis. 8, Figs. 3, Krefeld.
J a r c e v a M. W., L о t s с h D., N i e m k o v G. I. (1968), Zur Num m ulitenfauna des m ittleren und höheren Eozäns der Deutschen Demokratischen Republik. Geolo
gie, Jahrg. 17, 4, pp. 418—459, Berlin.
К de Siel Y. (1962), Die oligozänen Foram iniferen der Tiefbohrumg Dobbertim (Meck
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K i e s e l Y., L o t s c h D. (1963), Zur Mikrofauna des südbrandeniburgischen Obereo
zäns. Geologie, Jahrg. 12., Beiheft 38, pp. 1—71, Berlin.
K i e s e l Y. (1970), Die Foram iniferenfauna der paläozänen und eozänen Schichten
folge der Deutschen Demokratischen Republik. Paläont. Abh., A. 4, 2, pp. 163—
394, pis. 27, Figs. 8, Berlin.
M a r k s P., van V e s s e m E. J. (1971), Foram inifera from the Silberberg Form a
tion („Lower Oligocene”) at Silberberg, near Helm stedt, Paläont. Z. 45, 1—2, pp. 53—6 8, pis. 2, Stuttgart.
O d r z y w o l s k a - B i e ń k o w a (1966), O m ikrofaunistycznej granicy eocenu i oli- gooenu na Kujawach (Microfaunistic boundary betw een the Eocene and O ligo
cene in th e Kujawy Area). K w a rt. geol. 10, 4, pp. 1072—1078, Warszawa.
O d r z y w o l s k a - B i e ń k o w a E. (1973), Mikrofauna starszego trzeciorzędu w rejonie Sieroszowic (Early Tertiary -microfauna in Sieroszowice region). Prz.
geol. 7, pp. 376—377, Warszawa.
P o ż a r y s k i W. (1953), Osady morskie oligocenu młodszego na Ku jawach (Marine sedim ents of the younger Oligocene in K ujaw y (Middle Poland) Biul. Inst. Geol., 87, pp. 9—20, Warszawa.
S u b b o t i n a N. N., P i s h v a n o v a L. S., I v a n o v a L. I. —
С уб бо ти н а H . H., П и ш ван ова JI. С ./"И ванова JI. И. ( i9 6 0), Стратиграфия олиго- ценовых и миоценовых отложений Предкарпатья по фораминиферам. Микрофауна СССР, сб. 11, Труды ВНИГРИ, вып. 1 5 3, Ленинград.
W o l a ń s k a Н. (1962), Stratygrafia mlkropaleontologiczna oligocenu Polski zacho
dniej (Micropalaeontological Stratigraphy of the Oligocene of Western Poland).
Kwart, geol., 6, 1, pp. 149—156, Warszawa.
STRESZCZENIE
W iercenia w ykonane w ostatnich latach na m onoklinie przedsudeckiej między Głogowem a Sieroszowicami odsłoniły interesujący profil osadów trzeciorzędowych, w tym rów nież m orskie osady paleogenu. Szczególną
uwagę, ze w zględu na jakość m ateriału, bogactwo fau n y i ch arak ter przejść stratygraficznych, poświęcono osadom m orskim w otw orach:
S-382, S-380, S-365, S-350, i S-376 (fig. 1) z rejo n u Dankowie, Bukwicy, Jakubow a, Jerzm anow ej i K urow a.
M aksym alna miąższość osadów paleogenu w ynosi 96 m, średnio zaś w aha się w granicach 60 m. Z tego na osady m orskie z fauną przypada 54 m (w profilu syntetycznym ), zw ykle jednak w żadnym z otw orów g ru bość ich nie przekracza 30 m
Rozkład miąższości osadów m orskich oraz ich rozm ieszczenie związane jest z charakterem morfologii podłoża triasowego.
W profilu paleogenu (fig. 2) wydzielono osady rep rezen tu jące górny eocen (S-365, S-350, S-380), dolny oligocen (S-350, S-365) oraz górny oli- gocen (S-376, S-382). W większości otw orów b rak je st całkowicie osadów środkowego oligocenu. W żadnym z otw orów nie stw ierdzono także obec
ności pełnego p rofilu paleogenu. W ynika to z obecności pow ierzchni erozyjnych przypadających w różnych okresach wiekowych.
Eocen górny (14— 20 m) b u d u ją w przew adze piaski w apniste, glauko- nitow e i glaukonitow o-kw arcow e z fosforytam i, zaw ierające zw ykle bo
gatą m ikro- i m akrofanuę. M iejscam i (np. S-380) w ystępuje do 6 w kła
dek i w arstw w apieni glaukonitow ych piaszczystych, w apieni oolitowych i piaskowców w apnistych.
W niektórych profilach (S-365) zespół m ikrofauny (tab!:. I) skada się z licznych, ma ogół dobrze zachow anych otw ornic zaliczanych do M ilioli- dae (Sproloculina, Q uinqueloculina, Trïloculina, Spirophtalm idium , Lacazi- nella); Polym orphim dae, oraz innych np. Reussella sp., Biapertorbis bran- denburgensis K i e s e l et L o t s с h, Baggina iphigenia ( S a m o i l o v a ) , Asterigerina rotula haeringensis L ü h r, Pararotalia audouini (d’O r b i- g n y), P. inaerm is (T e r q u e m), P. lithotham nica (U h 1 i g), Cibicides carinatus (T e r q u e m), Cibicidoides bellus M j a 1 1 u k, a także nu m u li- tôw: N u m m u lites concinnus J a r c e w a i N. orbignyi (G a 1 e о 11 i).
Oprócz otw ornic w y stęp u ją w m ateriale pierw otniaki — Tintirm idae oraz szczątki innych organizm ów jak: m ałżoraczki, ru rk i pierścienic, ram ienio- nogi, mszywioły, mięczaki, kolce jeżowców, otolity ryb.
W innych profilach (S-380) znaleziono niew iele m ałych otwornic, n a tom iast liczne n u m u lity reprezentujące kilka gatunków . W zbadanym in terw ale o miąższości około 15 m, stw ierdzono też sukcesję gatunków N um m ulites ex gr. variolarius ( L a m a r c k ) — N. orbignyi (G a 1 e o t- t i) —- N. concinnus J a r c e w a .
U tw ory eocenu górnego w ykazują stopniow e i ciągłe przejście do oli
gocenu dolnego. Dla tego poziomu charakterystyczne są globigeriny ( M a r k s , v. V e s s e m , 1971). Znaleziono tu kilka gatunków globigerin, (tabl. II, fig. 1) w śród nich Globigerina danvillensis H o w e et W a l l a - c e, G. officinalis S u b b o t i n a oraz inine otw om ice jak S vratkina perlata ( A m d r e a e ) , Chilogiimbelina gracillima ( A n d r e a e ), Bolivina
fastigia ( C u s h m a n ) , В. tereta ( C o i s h m a n ) , Alabam ina w olterstorfii ( F r a n k e ) .
Osady oligocenu dolnego (15—23 m) odznaczają się w ybitnym spad
kiem zaw artości glaukonitu, brakiem wapnistości, nieobecnością w kładek w apiennych i m arglistych oraz kon k recji fosforytow ych, zanikiem n u - m ulitów oraz pojaw ieniem się drobnej m ikrofauny z udziałem otw ornic planktonicznych.
P rofil oligocenu dolnego obcięty je st od góry poziomem erozyjnym . Zespół osadów m orskich stw ierdzono po raz ostatni w dolnej części górnego oligocenu. W jednym z otw orów (S-376) znaleziono piaski k w ar
cowe silnie łyszczykowe z dwoma w kładkam i piasków ilastych kw arco- w o-glaukonitow ych (13 m), w drugim natom iast {S-382) osady ilasto-w a- pienne (8 m), zbudow ane z iłów silnie m arglistych z glaukonitem oraz 1—2 w arstw szarych w apieni m arglistych z ikonkreojami pirytu.
W otw orze (S-376) stw ierdzono liczne otworniice (tabl. II, fig. 2) z ga
tunków A sterigerina gürichi gürichi ( F r a n k e ) , Angulogerina gracilis te- nuistriata С u s h m . et E d w., A, gracilis germanica C u s h m. et E d w., Sphaeroidina variabilis R e u s s , Cribrononion subnodosum ( R o e m e r ) , P rotelphidium roem eri ( C u s h m . ) , M elonis affine { R e u s s ) . N ajw ażniej
szym stratygraficznie gatunkiem jes.t tu A sterigerina gürichi gürichi, w y stępująca stosunkow o licznie i w yznaczająca tzw. „poziom asterigerino- w y” zaliczany do górnego oligocenu. G atunek te n znaleziono rów nież w w apieniach z otw oru S-382, jed n ak tylko jako pojedyncze okazy w ze
spole z Cibicides sulzensis ( H e r m a n n), M elonis affine i E lphidium hil- term anni H a g n, co może sugerować, że w arstw y tu w ystępujące m ają nieco niższe położenie stratygraficzne w stosunku do profilu S-376.
U stro p u górnooligoceńskich osadów m orskich (S-376) stw ierdzono po
nadto w ystępow anie pojedynczych okazów radiolarii z rodzaju Ceno- sphaera sp. i Spongiom m a sp. (S u b b o t i n a e t al., 1960).
M orskie u tw ory górnego oligocenu przechodzą w sposób nieprzerw any w lądowe, węglonośne osady górnego oligocenu, a następnie miocenu.
G órnoeoceński odcinek profilu paleogenu, z uwagi na specyficzny typ litologiczny i ch arak tery sty czn y zespół m ikrofauny, proponuje się nazw ać w arstw am i sieroszowickimi.
W arstw y z Jerzm anow ej, zaliczone p rzez D y j o r a (1974) do środko
wego oligoceniu, w y d ają się być odpow iednikiem osadów m orskich dolnej części górnego oligocenu (tabela 1).
Akadem ia Górniczo-Hutnicza
Instytut Geologii i Surowców Mineralnych 30-059 K ra k ó w , al. Mickiewicza 30
R o c z n i k Pol. T o w . Geol., t. X L V l l z. 1
R o c z n i k Pol. T o w . G e o l , t. X L V I I z. 1
EXPLANATION OF PLATES OBJAŚNIENIA TABLIC
Plate — Tablica I
Fig. 1. The Upper Eocene foraminiferal assem blage (exclusive of Nummulites) (S- -365). 1 — Asterigerina rotula haeringensis L i i h r ; 2 — Pararotalia litho- thamnica ( U h l i g ) ; 3 — Cibicides carinatus ( T e r q u e m ) ; 4 — Baggina iphigenia (S am .); 5 — Pararotalia audouini ( O r b i g n y ) ; 6 — Biapertorbis cf.
brandenburgensis K i e s e l et L o t s e h; X 26,5
Fig. 1. Górnoeoeeńskd zespół otwornic (z wyłączeniem numulitów) (S-365), 1 — A steri- gerina rotula haeringensis Lühr; 2 — Pararotalia lithothamnica ( U h l i g ) ; 3 — Cibicides carinatus ( T e r q u e m ) ; 4 — Baggina iphigenia ( S a m o i l o v a ) ; 5 — Pararotalia audouini ( O r b i g n y ) ; 6 — Biapertorbis cf. brandenburgen- sis K i e s e l et L о t s с h; X 26,5
Plate — Tablica II
Fig. 1. Lower Oligocene foram iniferal assem blage w ith globigerines (S-365). 1 — Globigerina danvillensis Howe et Wallace; 2 — Bolivina fastigia Cushman;
3 — Chilogümbelina gracillima ( A n d r e a e ) ; X 65
Fig. 1. Dolnooligoceński zespół otwornic z globigerina mi (S-365). 1 — Globigerina danvillensis Howe et Wallace; 2 — Bolivina fastigia Cushman; 3 — Chilo
gümbelina gracillima ( A n d r e a e ) ; X 65
Fig. 2. Upper Oligocene foram iniferal assem blage „Asterigerina zone” (S-376). 1 — Asterigerina gürichi gürichi ( F r a n k e ) ; 2 — Sphaeroidina variabilis Reuss;
3 — Elphidium hiltermanni H a g n ; 4 — Melonis affine ( R e u s s ) ; X 50 Fig. 2. Górno-oligoceński zespół otwornic „poziomu asterigerinowego” (S-376). 1 —
Asterigerina gürichi gürichi ( F r a n k e ) ; 2 — Sphaeroidina variabilis Reuss;
3 — Elphidium hiltermanni H a g n ; 4 — Melonis affine ( R e u s s ) ; X 50
