Mid-Cretaceous events at the marginal part of the Central European Basin (Annopol-on-Vistula section, Central Poland)

lRENEUSZ W ALASZCZYK

acla:":

geolaglca polo"ica

.' . . ."

Warszawa1987

Mid-Cr~taceous events at the marginal . part of the ' Central European Basin

(Annopol-on-Vistula section, Central Poland)

ABSTRACT: . The lIlature of ,the mid-Or.etacoous. events . in the A.!lbia.n - Lower 'rUronian seq'\lellce expOiSed at Amlopol-Q[l-Vis1lUila(Centrail Polaind) 1s ttiscussed.

At least Jlour of· the ·:!live dilstingWshed here dieoontilIluilties

are

^shioWlIl! toO ^be OOrrelable with 'the eq'lilivalentalhenomena in other Pal:iJsh sectiOl!lJS and: with cOmmonly ;r~ized events. So, being eadier refeI'lred to the activity of, loocal upIdftilIlg movements ·of the AIIlIIlopol Swel:l, t-hey .axe .interpreted here as· the ~ob~

eVents record~ The adiV!iJty of the AIllnapol Swell was oIllly a favOl"aible :factor fOIl."·

the event expression through the 1imttilIlg terlI'ligenous influx, aiIIld jJt WIlliS

a!!i9o

res,ponsi!ble for the cOIIlde.nsation phenomena

m.

the. interva!ls between. The bathy- metiri,cal an.ail.ysils of the foramilndfet'lS Sihows thalt OIIlly one of the everuts (i.e. tl:~e

rriid-CenoanalIlia[I event) unquestionably ~s a eu:!itateevent, while the otlrers a'te ex.pressioos of both bathyroetrica!l' aiIIld chemical chamges in ~he mid-Cretac~

sea.

INTRODUCTION

Itappea:r;s wen .evidenced that the development of the mid-Cretaceous transgresSion was asSOCiated with a set of the ' widespread and approxi- mately isochronous events. The estahlished successi'on of events

is

valuable in paleogeographical and ecological interpretations, and it is commonly regar-ded as a promising tool in . stratigraphic correlations

(e. g.

CARTER &HAR'r 1977, HART 1980, ERNST

^& al.1983,

DAHMER

&

ERNST

1986).

Universal applicaHon IQf the "event-stratigraphY" · re- quires however further studies including evaluation of the isochroneity of events on a global Scale and also more i,nsight into their veJrynature.

The latter problem is related to a various sedimentary expression

oi

every particular event

in

contrasting paleogeog,raphicand fades settings.

This paper.:.coneernS th.e :.pr,oblem of 'r~ognition . iof~uiyalent events

in. : the .. strongly .

cOOdensed;micl~Cr€-tacoous

. section

e:1Cpose.d~t

Annopol;;;

.;orl::N~t1.lla Ha C~!ltfiiJ. . Pb!~~<l:~n~ iOcated' at the . ffiarlginaa part ofth~

62 IRENEUSZ W ALASZCZYK

Central European Basin (Text-fig.

1;

see also MARCINOWSKI

&

RAD- WANSKI 1983). This section on one hand is excellently suited, to -the event reOOgrution ' due to a lack of intensive teTrigenous sedimentation and preservation of rich fossil

assemblages"makil:lg,;~ea~acard

and precise dating of the global oceanic processes. On the other hand, how- ever, it was placed during the mid-Cretaceous on a swell structure, the

Fig.

1.

Geologic setting of the

Annopol-oo~

Vistula. region

A - Locaition of i'he studied arrea in Po1a:nld; HeM - Holy Oroos Mountains B - Geologic sketch-map of theAIlJllO}>O!l-on-Vi:stu~ 1t"~0Ill

C-D -"" Pa1eog~hre maps of Central Europedurmg .A.l1bi00i and Cenomanianl ITuronil8l!l times; asterdisiked is the -studied Qlt"ea (taken from ZIEGLER 1982; in C

milnor modwcaMon after MARCINOWSKI &'WIEDMANN 1985)'

ACTA GEOLOGICA POLONICA, VOL. 37 I. WALASZCZYK, FIG. 2

•

^/

z·

O:E~----,.l

DS5 - -

0::

^{~ --r---,-~}

* ( M. hercynicus) - -

:::l

^{~ 1- - . -- ..L...-rl}

I--

0 I---.---'---l

- ' I---'-~-"-I

1----l~....JI+-D 5 ,.-- z «

-~~DS3--

« z

o ~

z z

.. .r:::(

- al -J

«

1-r'~'\.~.--4

*(

A. jukes- brownei)

DS2 DS1

1m

OS

*

.... ^{.~ ". . . ~ ...}

MARLY

PHOSPHORITES

SANDY

PHOSPHORITES

discontinuities st rat igraphic gaps

Lithology, stratigraphy, disc·ontinuities and aSSlociated stratigraphic gaps within the mid-Oretaceous sequence exposed at Annopol-on-Vistula

Fi;eIld phot,o through the courtesy of A-s's.-Professor S. CIESLINSKI

- I

1 )

"

MID-CRETACEOUS EVENTS 63

actiVity of whicih could have been expressed

iri

a similar way as the preSUmed events. A differentiation 'between these two factors is the aim

of

the present study:

! . • . .

GEOLOGICAL SETTING

The·· mid-Cretaceous depositS' (Albian - Turonian)

of

the studied area, near Annopol-on-Vistula, are exposed along the limibs of the Laramide anticlinal structure, and they

Test.

with a slight angular uncon- formity

(1_2°)

upon the Jurassic {Kimmeridgian) substrate

(see

Text- -fig. 1A...,...B). The mid-Cretaceous depositS represent a typically trans- gressive sequence. Starting with the M1ddJe Albian near--shore sands

and sandstone, the 'sequence passes upwards into marly sands and marls of the Upper Albian and Cenomanian which, in turn, are overla1n 'bY

alniost pure · cairhOiDates of the Turoriian (Text":fig. 2), The very cha- racteristic components

of

the Annopol section are nodular phosphateS Of . the · Middle - Upper Albian and ·

t~e

phosphatic

minerali~tion.

asso:..

ciated with the Middle and Upper Ce'Iloomanian haIrdgroWlids. Single phosphatic nodules occur also in sandy glauconitic marJs of the Lower -, Middle Cenomanian and rarely also in the Lower 'l'uIronian maT Is.

The Annopol section, occupies an exceptional position among the extra-Carpathim mid-Cretaceous sequences of Poland, which are com- monly characterized >by the intensive terrigenous sedimentation. This situation aroused froom the peculiar paleogeographic

^s~ttinJg

of this a'rea during the mid-Cretaceous,

viz.

its position

0'1l.,

a swell structure (the Annopol Swell -,

^see

CIESLINSKI

1976,

MARCINOWSKI,./}L RADWAN- . SKI

1983)

rising within the axial part of the Polish Danish Trough

^(see

Text-fig.

le-D).

BIOSTRATIGRAPHY

The hiostratigraphic position of particular lithol'Ogical units of the AIliIlopol sequence has ; been studied earli€'l' by SAMSONOWICZ

(1925, 1934).

POZARYSKl

(1947, 1948, 19~6),

CIESLINSKI

(1959, 1976),

and recently advanced thoutoUlgl11y and summarized 'by MARCINOWSKI (1980),

MARGINOWSKI &

RADWANSKr'·

(1983),

. MARCINOWSKI

&

WALASZCZYK

(1985),

and MARCINOWSKI.& WIEDMANN

(1985).

The stratigraphic

subdivis10n

applied in this paper

is

in agreement with the last four cited papers (MARCINOWSKI

1980,

MARCINOWSKI

^&

RAD- WA!'JSKI

1983,

M,ARCINOWSKI

&

WALASZCZYK

1985,

MARCINOW- SKI &WIEDMANN

1985)

and the reader

is

referred to there for detailed stratigraphic data.

J

~RENEUSZ W;~ASZCZY~

~

. . ' .E:lfceptE:d

iS~l:o-w~v.erthe·

CenomanianlT1,lfonianboundary whicp,

^.c9n~

tr:ary~tCl~previous.

opif:lions" d(}eg"not

repres.~t

§LOO!ltinuoUB deppsition and

is

mamed by a sedimentary break with a stratigraphic gap;

1\io~E;!<

over, a stratigraphic gap

^is

also confined to the LowerlMiddle Turonian boundary and is associated with the haroground. The lack here

of

Mytiloides hercynicus (PJ!:T,!tA§:CHECK) , indicates the gap comprising the upper zone of the Lower Turonian

in

the bipartite division of this supetage, (i.e. ,. into ,

My

tH oi des . . mytiloid€S and

^{Mytilo~des .}

hercyn.ieu.s

ZoneS). .-: .

. .

.', . LABORATORY· DATA

'_lo.

. The

fiel<dw~k:s'for

^{th'f;) .}

~~send;

^study

wer~

cam'ied out iIn 1983-1984

a~s ~ ' part

?f

the'gIradurutepc$er <VV:ALASZCZYK 1984). . . ... .. . Laboratory .studies . included petrQglr8IPhiKlal ilnvestigati-cms based on ~Od;hin

sedtions, XRD-aJrlalyses of phOl~orites, aJil.d a micropalleontologkstudY. The plalniktonlbelnthos raltio gm,ph (see Text-fig; 4) was !Plotted basing 0IIl 17 .sa'llllPles,

w~th 200's:pecimEmls ;coWllted iJn every sampl.e (the 1'oweslt thr:ee samples 8lI'e excluded becalll!Se af low frequEmlcy ·af fOlI'81roinafers). The XRD-amaJy,ses were peclormed iIn

the Geological SUiI"vey of p,oland .

. " SEDIMENTARY RECORDS

. Five

disoontinuities may

be

distinguished

in

the seeti,oo exposed at Arunopol ... on-Vistula, represented either by distinct lithological boundaries or by . har. dgr· oUiIld hori' wns,

to·

which stratigraphic gaps are ' confmed (Text-fig. 2). The intervals between 'are the :oondensed units with rework-

ed and mixed sediments. -

Discontinuity No. 1

!t

is

placed within the Albianphosphorite bed sepaTating the smdy phosphates .of the Middle -1ow-Upper Albianand the marly phosphates of the uppermost Albian (Stoliezkaia dispar Zone). These two kinds of ph:osphates differ macro- arid

mi~roscopically.

.

The Middle- low-U~rAlbian sandy phOSlP~tes form 1uge ~u:p to 20.CIll1 liIi . diameter) spindle-shaiped, .light

to

~k lroown phosphocla$ts CompOsed .of dens!y paicked quaIitz, glauCOill-ite, dubm-d!Jnately fe1ds~ and cha[cedony g,raiJrus, cemented with· milcroorYlSfuUilne f1uorapati,te :.(see rndcrophoto in Text-fig. 2). ^No' microfaUilaJI.

tests were folIDtl iIn thin sections. l1he maorofauna :is cOIIllPosed of ammonite moullds am she115 and alsClSPrur;s~ jJn~am· fragments. There 000UlI.'" also wood .:fu"agmen~,

phosphati:red and bored by the bivalves Gastrochaena BP. (PI. 2., Fi.g. 1). .

rhe uoppel-most. Mbia!Il rnarly phOlSiPhate.s are COmposed ofsmalJ.l (oommonlly leSs than 1 am Jnddameter)' light to tdail"'k brown ph.osphocl.a.sbs, many of which represent p,hosjphatized fosshl moulds., cemented into larger ag.gregates. The IPhOs~

phates are matrix-supported mic["o- Ibo CIl'yptoc.rystail.lilne phosphates. with a varying

ACTA GEOLOGI'CA POLONICA, VOL. rr I. WALASZCZYK, PLo 1

1 - Mfd-Cenom.anian ha,rdgroull1:d (Di'5'cOIllrtinuity. No. 3) and !j:lhe ov,erlying sequeruce:

Upper 'Cenomaniaul mall"ls - Dis'CIOintinuity No. 4 - Lowetr Turonian limy

'ma'flg; ·u:ruder,gJr()UJnd gaUery 0I.f it'he abandoned JPho::lPhOirite mine at An.rlopru-OJ1-

-VistuJa

2 - DiS'Co.ntilhuity NOi.

4'

vhtih U~ Cenomani:an mads beneaoth and Lower Tu- TOtI1iaul .limy marls albo;ve; ulI1dergr·oUtl1d gatl1ery .of the abandOned phQsphOiriote mine a;t Ariln¹qpol-Oin-Vi"Slttul.a

Both photcs through the courtesy of Ass.-Proiessor S. CIESLII'l'SKI

ACTA OEOLOGliCN 'POLONICA, VOL. 37 '!-.-'WALASZCZYK. PL'; 2

1 - Phosphatized wood fragment bored by the bivalve Gastrochaena sp.; lower part of the phosphorite bed (Middle - low-Upper Albian)

2 - Lag intraclast with serpulid encrustations and glauconite veneer; mid-Cenomanian hard- ground (Discontinuity No. 3)

3 - Phosphatic ooid with quartz nucleus; upper part of the phosphorite bed (uppermost Albian - Stoliczkaia dispar Zone)

4 - Crypto- to microcrystalline phosphatic matrix of marly phosphoclast; upper part of the phosphorite bed (uppermost Albilm - Stoliczkaia dispar Zone)

5 ~ Lag intraclast with burrows and phosphoclasts, glauconitized and phosphatized at the surface; mid-Cenomanian haraground (Discontinuity No. 3)

Photos 1, 2, 5 in nat. size; taken' by S. ULATOWSKI Photos 3 X 70 and 4 X 40; taken by J. MODRZEJEWSKA

MID-CRETACEQUS EV~~!'I 65

matrix/grams ratio (PI.' 2, F.ig. 4; Bee alBO milClOOphoto in 'l'ext-fdg. 2). The grains, besides the domilniaJtiing

quadz

and gIaucon.ite, axe coo:nposeid of ph()l,';ij)hatic pel1ets, ooids (Bee PI. 2, Fig. 3) and differently lPl'eSle1'Ved mLorof,ossd.l tests, primaa-uy planktic foraminrifers of the genus Hedbergella.

Besides the areas with one, dilSltindt phmphOll'Lte bed (eastern pari of the NE margin of the Holy CrOSiS Moun~, ailS() Ibhe liuIblin UlPland) 1110 eqiUd.valents of this diOOl1itllnuilty may be indicated in other ,Mbial!l sections of Poland, as they are commonly represented by the continuOUls 6aIIldy sedimentation, and their falllllistic docu'1OOIlltation is utrlSUfficlent'to make

any

time detarmialation.

Discontinuity No. 2

It forms the b0'Undary

betw~en the Albian phosphorite bed and the LowE¥" Cenomanian sandy

g~auconitic" m~rls.

This discontinuity was firstly reported by CIESLINSKI (1976)

,who'

suggested also a strati- graphic gap at this boundary, Comprising the Lower

and

?l'Ow-Middle Cenomanian. However" basing on the ammonite' assemblages MARCI- NOWSKI (1980) showed this assumption to be groundless.

The A~bian/Ceno:maJOdan boundary ~ aloo 'Shairply !!ll&'ked !in other mid-Creta- ceous !Sections of Poland. 1111 the Polish Jurailt iJS maa.-ked by :the~'I'ance of cailcium calI'booate OOIl1tent (MARCINOWSKl 1974). lIIl the SW maJrgin of the Holy Cross Mountains, 8C<ilngloaneratic band is mehti'Olneld aIt this time

mtervaa

(HAKEN- BERIG 1969, 1978), and along the NE mar~of ,ft/he H01y 0r00IS Mountadm thiis boundary ris placed

at

the upper surlalce .of Jthe phosphO'I'ite bed;s.i:mllarly as in the Alnlnqpollseclion (Bee e. g. CIESLI~SKI 1959). '

Discontinuity No. 3

It is

expressed by a oomposite hardground horizon. terminating the Lower - Middle Cen'Omanian sandy glauconitic maxIs (Text-figs 2-3, and PI.

1,

Figs

1-2), with a thick (up

to 30

crii)ha~d ,paa:-t,and

with

glauconitic and phosphatic minera1izations (PI. 2, Figs 2, 5), encrustations (Pt 2, Fig. 2), and complex genetical history

(lSee

Text-fig. 3). DiscOn- tinuity No. 3 was firstly recognized and mterpretedby POZARYSKI (1956) and the associated strati-graphic gap, comprising the Acanthoceras jukJesbrownei Zone, was postulated by MARCINOWSKI (1980).

The diiJSoussed d.il&COlrlltintuity is aocompalllied aolso by a dilSlt.ilncl rlse

at

the pl8lIlktonlbenthos 'raJtd.o Within fm'ammffer8dassernblages, although

its

sedimen~

expression (h~0UI11d develQPIIle!l!t) .is rarely observed in other secti.oIruI. A :radicall.

increas~ Qf the pl'8lIlkltic fO'I'aamndiers fu1equency of the same age

is.

hQWevet', coon- , 'tMniyobSeriedin:

the other

CenoIn:imlan

sectiOnS

Of

PbIoWiul

(HUSS 1962,ZA'PA.

t.QWICZ~l3ILAN,1981, ,GAWOl,t.,.BIEDOWA1982)... " ~'" , "

. . ,. - - - ." .~ "'". . _. . . :.... _.' ," . I . ' '. ,. . • •. ,

-' It' ;is'

represehted' hy: a well ' rtianif~ed ' dhl~iOOi'surfacea,(the 'tot>

ot the haevily,

glauconiticUpper~Oen?JXlanian mm-Is

(.see

,

PI. 1,Figs 1-2),

and

" is :ov~ladii.

by limy :nilll,'is ,'ot, : t<>wer. ' ^Tj,troni@

^•

age. ' ,If

w~fil'S1t~y

IepOded~"by;;p6ZA-RYSKl

{1948),

an~ ~a ':'straiigraphi~~ gap~~,,'sUggest~

bfCIE'SLiNSKJ'(19'16):~ L >:,,} :' ", . ~ , .. " . ;-, , .' ^, .::- ~ .. :.. ... ^~:. ,. ,.:: .:. :..

...

^{~ .;;':. -:} -.; .. :. ~. ".' ~.,: ':~ .. -~ -:;. ^{"' ..} "

5

.!._--_ .. _ - - -_ .. __ ._-

66

I.REm:u82: W ALASZCZYK

' Eig.:.3.DevelQpmentoi- the

mid-CeporQ.~an .ha'l"dgvOund (taken from:

.MARCINOWSKI

&

WALASZCZYK 1985, Fig. 2)

4, ~~~~~~ '~:;~ ~ ~ ~rthe :~~e"C~~i8n(includmg ~

TurriJiites acutus

zone)

^{0 • • • • ••• ~. • • • . •• ' • • '. •}

B - Break iIn oodiImerlItation (AmrIIthiocerasjlUkes'lio\wieiZolne) with' erosion dOlMl to Lower CenIOIrnanian dEfPOSits: phosphaitizatioo of tllOldds, sometimes alsQ of sheIds; formation of the :residuail !lag .

~.-.Non-d~td.on period; 'settWlg of tlbe 'bWrIrowillllg faUlIlaarui incipient Bub-

o . 'IStl'aIte 'cementation . . '" .

D ... Vetli sl,aw sediIru;m.tiltian; fillmg of burrows rih new seld!iment as we11 as . with ISIIIlaIH ipalitioles (up to 3-,4 cm

m

<tiameIier) of the residuatl Jag . . D' . (alLtemative) - Like D, 'but '\Without fiilling IO!f bUtl'l'ows by the residual. !Iag . ;';.

B' -

EtoisiOnu!

~iOOde;.bOIriIlg, eIlCrn.lSting ··of phalphatic nodUles, and·impreg1oati.oo Wli:bh ip~haItes and gIauoonite of the eroded Ibani subsIttraItai fmgmeaJts

(formation of hiaWs ccmcretioos) .

;MID-CRETACEOUS' EVENTS '67

Except 6~e' examples of· ,the conit:inu~ depq.c;ition QC1"O¥ this· bounda!'Y. _ in other parts of Poland (e. g. Glan6w 1SeCt1i<lttl :in the PoI1dsh Jum, Bee MARCINOWSKI 1974); it' lS commcmly

mUked by

cOru:1ensaJtion hor~, ~nd9,' clay ,layers (see ClESLmSKiI & P02ARYSXl' 1970; ClESLr:&SiKI &JASKOWlAK 1973; HA- KENBERG-1969; 1978; MILEWlCZ'1959, 1963), and other dilStmct !Hthdlcgicail. brealks

(M;ARClNOWSKl 1974);' '

Discontinuity No. 5

- '-

'It

is a hardgiI'ound horizon (initial hardground sensu KENNEDY

&

GARRISON

1975)

with the well defined 'Thalassinoides-type

bUlTOIWS;

usually weakly glauconitized. This ' Lower Turoniain hardgr,ound with, an associated sedimentary gap, of unprecikd. stratiJgraphic extent, waS

fitstIy reported by POZARYSKI

(1948).,

This gap comprises. , the My-

tiloid€S hercynicllS , Zone. '

"'~

, !

The bouOOairy"l:liErtween, the Lawer 8ItId Middle Turandan ;is'

disfli!!l~

ⁱⁿ

a~t

eve:ry IsecidO!Il .in Poland where the depositsorf boith these SIIlbstagei; I()C(:ur

(see

BUKOWY 1956, MARCINOWSKI 19'1'4). The stating however, about ilts time-equi";

V'al1~ :with thiS diSlOOlIlltiirooity in oflhe AmlqpOl section is diUicWt, as the ~

~8IIl sequence in PolaInd is ll10ISt common:ly I00I;' suibdivided IDto the two ber~

d~hed zones. Firom the QW'll experiMce iIit appewrs that the majority of . il,le d~i1ls ,~ed ·to the lnceramus labialbus Zone (regarded as

the

equiva!1ent

- Of'

the

LQwer

T,UIl'onian) belong to ,the MytiiloidelS mytiloddes Zone (e.' g; \ in ,the PolIi:sh

JUIl'8, tl1e Crnoow Upland in~ludin1g). '

, BATHYMETRICAL CHANGES RIECORDED BY FORAMllITIFERS

-:TJl~

interrpretati·on 'of bathyme1Jry at which the studied' deposits were laid" -down

is ha~ed.:.()nrelatiVe

- changes'of"the planktOln/benthos ratio and' on the distrihu.tIoo· ⁱⁿ the--,profile . .g£planktic foraminifers depth g;oups (Te~t-fig.

4),

s.:imilarly as given

in

1Jhe referenced

papers

(GR~MS­

DALE'

^& yan

MORKFl.OVEN

1955,

HART

^&

TARLING

1974,

CAR!l'ER

&

HART

1977,

BE

1977,

HART

&

BAILEY

1979,

HART

1980, ,1983);;

. . .' .'" 1

The actual distribution

of

foraminiferal assemblages ill the AnnopOl

Sf!Gtion

is, strongly IDfluenced by secondary f.actors, mairuy vertical displacement .of tests anct-homogenizatioIiof the deposits

^'<i~ ~t<:>

activity of burrowing infauna. A downward introducing of the 'niierofauna

is

paxticulaTly well evide.IlCed

in

,the Albian,'wbere the typically uppermost Albian 'species Ot, Rotalipora occur

in'

the unquestionably".l{)wemnost Middle Alb!8!I:l

~ands,

just be1.1.eath the phosphorite bed (see

Text-fig.',~).

In these sangs

~l:1e

forar$lifer:s

~occur

only in the uppermost

(30

cm

~~)

b1otu.rbat~,d-,;pa~(

'Mo.rem,er, ' as" the foraminifers d.o not OCcur ID

larrge~

... ~.~"'" ~-.~:.' ," -<-~'.,: .:~~; ~> ',...... :.~ •... .'.'" ~ .

• ' .'V-, ",: .. ' .... ' .. ' ... : ! ~ ,'~ ..• ,. .. ^{... , i '" .c.... • . . • ~}

i

r- . t

, ,

i 1------ --- - - --

68 mENEUSZ, W ALASZCZYK '

sandyph(lSplioclasts

hlit':only' inthe::iharly: emes, theit initfalrange must

h'ave 'been'

i~ted'

'to

thi,'

upper ' .Part:, of , the,

ph~horitebed' and, ,: lat~

theYlUi\r~6nli'~e~i.Lir~nSportM doWhwam ; (se~ Text~fig: 4) .. " , . , "

,"', Si'rriilarly,in tlie'fil1~gs::,

^of

bunrows:beneath , the b~~~uity No~3

(mid-Cenomanian hardground) there occurs a foraminiferal

assemblage

z

Ill(

o :E

Z III

U

~« ,

,

:Q

^{..;.I' ' ,}

. - ..J,

o:~

OJw

«

D:

~ '

o

depth '

•

o

Fig~ 4. F~r~iD.ifers

in

the m:id-Cr~~eoU8sectiOnat A~opOl~-

Vistula A - Distribution at the selected piaokItdc foraminUers; white paris of :the ranges

are'the intervals of see<mdairy'iJnItroduci.ng B - Planktic!benthic ratio graph

" :, ,,"':_~c":"""";Jnterpt~ paleQd~ of the tnid-Ctet'aceQUs'sequence' , ' ' J '

1,)"_ rDi:&tributkllll ot lP~e f~~ depth: gtl11JiPS '(CJ#J!r ;HART -& BAILEY 19'19) ;,:::';", :: ,,' .. __ , ." ;

MID-CRETACEOUS: EVENTS 69

with a' bundalllt

Rotalipora: cu:shm~m , (l\{9R!tO~W)

being different from that occurring

in

the surrounding sediment (see Text-fig. 4).

'

} ,. The

;most

,probably the , activity , of the infauna is .responsi'ble

also'

for theoocurrence,

,in

the, Upper: Cenmnanianma.rls, of manyplanktic

for..:.;

aminiferscharacteristiC" : of the TtiIonifin. {see Text-fig:

4),

'asm:ay ,:be judgedfI"om :thebtuTo-ws descending from the Turoruan 'marhi into the ppp.er CenomanianheaVily' gluconitic marlS (see PI. 1, Fig' .!). ' .. , ,.

'"Any marked , contribution

of

the plankticforaminifersto the whole foraminiferal assemblage, being rather, low , ' in its Albian -

Middle

Cen'Ollianian mterval,

is

'confined to the upper part of ,the profile (B

~n

Tex't,;,fig.

4).

In its lower pai't,a sma:ll

peak' Only-is

observa-ble

in

the Upper Albihn phosphorite-bed;

It is

aSsociated, hOlWever, with a

fre-

quency increase : of the , small, globular hedbergemds, and so of ' the shall-QW,..marine,

forms.

This may suggest an increase of the: stirlace water productivity rather than of the water depth. Such initerpretation

is

supported by recent observations of the

high

organic production of the surface waters over the phosphogenicareas (BATURIN&

13EZRUKOV 1979; CooK'~

Mc, ELHINNy

1979).,

: A

rapid inorease of the , plaI1!ktic , fQraminifers content

is

related

(B ' in , Text-fig.

4) to '

the mid-Cenomanian hardground i(Disoontinuity

No. '

3).

In the fillings

of

bUITOws descending to 'about

1 m

down fTom the hardground the plankton/benthOB ratiols about

30%

with the rich oc::cuq."t:mceof Rot,alipora cushmani and Praeglobotruncq,na spp.

, The m'OB,t impressive is the Upper Cenomanian peak, .;lSSociated also with,

theappe~ance

of the deep water imor'phortype8

of the

plqnldic

, foraminifers. However, at least part of them

could

have been secondari:ly

introduced here during , Lower Turonian time. Moreover, an important role, CQuld have played the ecological

fa~tors,

namely bottom conditions nO,t , well-suite::i fQr OIrganic life, what is indicated by a radical decrease

of thebenthic focaminifersdiVl&Sity, ' and rby an aIlnost OOmplete lack ^'of

thebenthic (and also nectic) macrofauna, , though it abundantly occurs both below and above in the seotion. This Upper Cenomaman

cr~is in

orga: nic life is the widespread

:~ent()llllen'Oon,

and its cause was a subject

of " diversified' , iriterpretations (see HART

&

TARLING

1974,

MARCI-

NOWSKI

i980). " , "

' 1"0

sumniairli~,'

basing an theforaminiferal analyses a distinct sea level rise may be suggested for the Discontinuity No. 3 (mid-Cenomanian haroground) and less distinclly also for the Discontinuities Noslaild 4.

No ^chan' ge in foramihiferal aSsemblage which could be interpreted as a irespcmseto the sea level rise may

be

attributed to the Disoontinuities Noo 2 and 5. A decrease , Oof the ratio after the Albfan and Upper CeniO- manian Peaks may hardly be interpreted as the shall owing

of

the sea as these peaks' were ecologically ' controlled, and

int!he

case

of

the Upper Cenomanian

peak

it

~

'also of ta' phonOomical nature. _ :

. i , _ . _ - - - -

!-._ . . . _ ...

~----

70 lBENEUSZ WALASZCZYK .

GLOBAL:rNTERPRETATION

Disoontinuities

and~iated

oondensation

.'phenomena, '

reworking ' and hal'dground. fQl'lllation were reported

in ail

the earlier surveys an th€ Annopol section (SAMSONOWICZ 1925, 1934; POZARYSKI

.

19.48, 1956), being ascribed later

to

the

actiVity of

the Annopol ,Swell

(e .. g.

CIESLINsKI 1976, MARCINOWSKI

& 'RADW ANSKI 1983). However,

equivalents of the here recorded disoontinuities are more or less variably recorded alsQ

'in

other mid-Cretaceous

' sections in Poland. Moreover,

bas, ing

'on .the ·

detailed stratigraphic framework in

.the study area (MAR-

CINOWSKI 1980, MARCINOWSKI

&

RADWANSKI 1983, , MARCINOW- SKI &WALASZCZYK 1985, MARCINOWSKI

:&

WIEDMANN 1985) possible is also their correlation w1th the same age phetnomena in NW Europe. This suggests that they shoUld he referred

,to

the widespread mid-Cretaceous events.

,

The most striking example

is

the mid-Cenornanian Disoontinuity No; 3 with associated rise ·of the planlclionlbenthoo ratio indicative of a deepening ,pulse

(see

Text-fig, 4). ThiS is isochronous with the

·

wide- spread; so-called mid-Cenomanian non-sequence, recognized on the for- aminifera,lassemblage analyses by HART & TARLING (1974) and sub- sequently reported from Europe, North Atlantic and North America (CARTER

&

HART 1977; HART & BAILEY 1979; HART 1980, 1983;

DAHMER & ERNST 1986).

It is

noteworthy that at

this

very time the mid-Cretaoeous transgreSsion encroadhed the Sudetes from NW (MILE- WICZ

1959~

1963; S. RADWANSKI 1966) alIlid this well evidences the mid-Cenomanian eustatic rise:

,

SimilalI'ly, except of the

'

DisOOllltinuity No. I, associated probably wt.th a .rise of the sea leVel (Text-fig. 4), the rest three- may easHybe correlated with theequivaleDJt phenomena in west Germany or England

(e.

g.JEFFERIES 1963, KENNEDY 1969, SEIBERTZ 1979, ERNST

& al.

i984,

.HILBRECHT 1986), wlhere they are inlterpreted as the eUStato-

events, though wiili. different opinions on the direction aJIi,d nature of these changes

(compare

HART 1980, ERNST

& al.

1, 983). Basing on. the

Annopol

example, Uttle may

be

said) in W eSSe and

onlY'Q,t 'tl$

CenomaDJianJTuronian .boundary a deepening pulse is

assum~~ (see

Text-

-fig. 4)..

.. . ,

.

. , ..

.

..

I'llStead, O! importance

in

looking for a na, twre of particulcy; events :rn.ay be the,Jact of correlation,

i~

time of

th~

DiS(:onti;nuity No., 1 with

t.h~widespread

and short-timed

Cenomani~nr;ruronian

bound.a1-y anQxic event

(e. g.

SCHLANGER

&

JENKYNS 1976;

,

JENK,YNS 1980, 1985;

de BOER 1983; HART

.&

BIGG. 1982). This event, though differently

interPreted as about its origin, ' charracterizes a special kind of oceandc

circulation with a crisis of carbonate sedimentation (de BOER 1983).

MID-CRETACEOUS mVl!:NTS 71

Th~,

at .Amlo.pol region where the terrigenous sedimentation was

~~:rongly

limited, ..

the crisis

of . carbona.te prodU'Cfion

oould have

led

to

the ncm-depClSitiOrutl conditions and to the

form~;tionof

the discontinuity .

.

"

.. CON.CLUSION

,

At . least f'Our . of the five disooniinwities Observed in the Anno()pol

sect~,cm,

well conelable with the equivalent phenomena

in

other sections in Poland and

in

far-distant regions, represent the

irooo~d of

theglo'bal mid-Cretaceous.events. DiSoontmuity No. 3

is

tlnquestiQnahly . eustatO- event while the- others are p.robably (If

more

complex nature though in the case of Disc;:ontinuities Nos 1 and 4. bathymetrical changes are also assumed.

The activity ofttie Annopol Swell w:a.s 'OnJy

a f.avoraJble

factor through hampering the.terrigenous sed:imen:tation,as it mUSit be kept

in

mind that any event expression requires propitious local sedimentall"Y conditions, and in areas with intense local tectonics or high terrigeoous influx _ there

is

little

^chan~

of its record.

Acknowledgementfj ^..c.'

. This paper to a large extenlt ;ba5eis on .the graduate paper pe:rfarmed in the msti!tute of GeOilogy, University of Warsaw, OOder eupervislon of Pl'ofEssor H. MA- KOWSKI and Ass.-Prof~ R MARCINOWSKI to Wlhom the warmest thaJllb 8Ire offered for their oonstaM en-cO\lJ.'8gment, ,suggestliiOOls aIlld fruitful diiscussions, and to A-ss.-P:rofeSIsar R. MARClNOWSKI also fur a crIi.<ticall readmlg and improv-

ing an earlier dradlt of the typesc.rjpt. .

Moreover, hearlfelit thanks are- due :to ProfesSOIl" A. RADW AN'SKI (I:nstitute rA: Geology, Univet'lS.ity ·of Warsaw) aI!ld to Dr. M. NARKIEWICZ: (Geologicail Sua"vey

\iJfPoland; W8II"ISaW) for suggestions which OOMid~b1y imlProved tihe text.

Institute of Geology 01 the Unwer.fttt 0/ WaT8aw.

AI. :twirlet t W!gury l1li,

. 02.,089 Warszawa, potand

REFERENCES'

ili

1'\(; . . .

BATlrnIN. G.' N. & BEZRtiKbv~ P. L. 1979 .. p,hosiphoriltes ^0IIl the .SEIa!' floor and . their origdn. Marine Geology, 31 ta0.4), 317-332. Amsterdam.

~, A. W. H. 1977. An e-coq.ogica~, zoogeographic am:l ,taxonomic treview of' recent ' iPLaOktOlI1i.cFbrami:nifam. In: A. 'l'; S. RAMSAY (Ed,), OceaIIlic Micropa;l.eonlto- .. 1ogy, Vol. 1, PIP. 1-100,~ Academic Press; Loaidon. .

BOER de, P; L. 1983. ' . .Aispecfls of Middle Cret8lCOOllS pe1agic' iSeddm~t.artdIOIn . iJn sQUthern EwrOlPe. Geologica Ultraiectina, 31, 4;;104. utrec'hit.

BUKOWY,' S. 1956. Geo'logy tl'f. the area be't(ween. 0ra1(!QW and KOO"Zkwia., Bi1l,1. Inst.

Geol.,l08; 17.,82~ Wars:zawa; . >,'.:: ,.' .. ,. !.':': "":c. '., ".-'

CART;ER,. DJ J:. & ~AR'l'" M .. B... 19,7'l. AiSpects qf mid-Cretaceous stmtigiraphdjcal micrqpaleontology. Bull. Br. M:'Uos. fiat. ;tJi.s.t. (G~oL.) 2~,(l,), 1-:-1:35. LoodlOln.

72 ^IRENEUSZ· W ALASZCZYK

CIESLI1:rSKI, S. 1959. TheAlbim and Cenrama.niam Iiin. the northern. periphery of the Holy Cross MoUllltams.. Pr. Inst. Geol., 28, 1-95. W8Il"'SZaWl:ll. . - 1976. Deve[oprnent 'of the Darush"":"'P01Wi F\mr.QIW :in the Hoiy CXOSlS Region

:in the . AI'bian; Cenoma.n.iaJnand· Ttirobiattl. BiuZ. Inst.· Geol., 295,· '249-271.

War.szawa.

CIESLmSKI, S. & POZARYSKI, W. 1970. CretaOOOlliS. In: The stratlig!raphy of the Mesozoic Ijn thema/l"gdnoftheHolyCrossMOIUlIltailIlls.Pr. Inst. Geol., 56, 185-235,. WaJl"'szawa.

CIESLI1:rSKI, S. & JASKOWIAK, M. 1973.Ka.-eda. In: Budowa GecJ.logiozna Polski, -tom 1, St!l"atygrafiia, cz~§c 2 (Mezozodk), [In Polish]', pp. 580-615. Wyd. GeoZ.;

. Warszawa. ,

. COOK, P. J. & MoELHINNY, M. W. 1979. A reevaluatiOlll of the SiP6Jl;iaJand tem-

poral distribution of lSedimentalrY :ph<l6tPhaote depc:ll9i1ls in the Joight of plate . . . tectoruics. Econ. Geology, 74 (2),315-330. Lan.caJstar.

DAHMER, D. D. & ElRNST, G. 1986. Uwer Cretaceous Everut-,stratiiraphy :in Eurqpe. In: SummalI'ies of 5 Alfred Wegener OOIllference and 1st Int€rnat.

WOlI.'kishop of the IGCP Pr.oject 216 "Global Bioevents", GOtt.ingen 1986, pp.

23-28. GOttilngen.

ERNST, G., SCHMID, F. & SEIBERTZ, E. 1983. Event-Stratigraphy im Cenoman und Turon von NW -DeultschJ1and. Zitteliana, 10, 531-554. MOnchen.

ERNST, G., WOOD, CH. J. & HILBRECHT,. H. 1984. The CenOInaiIllaln - Turonialll boundary pro1:Jlem in NW-Germ8JnY wilth comments on the nooth - SIO'Uth correlation to the Regens'tllm"g Ao:ea. Bull. Geol. Soc. Denmark, 33 (1-2), 103- 113. Copenhagen.

GA WOR-BIEDOWA, E. 1982. Biosintigralphy of the AtbUin,· CooOlmaJnianand Turonian deposilf;s of Western and Cantral PolaalJd baised 0Ill the occurrenee of focaminifera. Biul. Inst. Geol., 329, 63-131. WQ['ISZQwa ..

GRIMSDALE, T. F. & van MORKHOVEN, F. P. C. M. 1955,. The Mitio between pe1agdc and benthonic forami:nifera as a means of estilmaJt:ing depth of depci.c;i- tiOln of ,sedimenltaJry ll"ocIkis. In: Ptroc. 4<th World Petrol Congr., Sec. lID, 4, ,:RP. 473-491. Roma.

HAKENBERG, M. 1969. ,Mbdan aIIJId

ceruomanialn

between Malotgoszez and Stanie- wice, SW boirder of the Holy Cross MOUIIltainlS. Studia Geol. Polon., 26, 5-126.

Waa-szaWQ.

- 1978. Albian - Cenomanialn ipaIaeotectOlllios and pailaeogeography of the Miec:h6w depression, lIloothern 1P6Jl"!I;. Studia GeoZ. Polon., 58, 5-103.. Warszawa.

HAR'l', M. B. 1980.. The ~1liIon. of the mid-Creta1CeOUlS sea-level ehanges by means of f<;lram1nif€l"a. Cretaceous Research, 1, 289-29'1. LOIndOlll. .

- 1983. PiJ:aJIlik1xmie foranidnifera fr,om the Cenomanian of the W~

qUa1'1l"ies (S. E. DaV'on). Proc. Ussher Soc., 5, 406-410. London.

HART, M. B. & BAILEY, H. W .. 1979. The distrtiibultion of iflhe lPlaJnktonie FoIr- aminifexida illl the mid-Cretaceous of NW Eu!l"qpe. In: J. WlEDMANN (Ea.), As:pe:kte dar Kreide Eua:opas, lUGS Series A, 6, PP. 527-542. Srtutbgiarl.

HART, M. B. & BIGG, P. J. 1982. Ainoxic evenJts_ in tlhe Late cretaceous chailiks of North WesIt EUJrope. In: J. W. NEALE & M. D. BRASIER (Eds), Mdw.o- fossils from Recent and Foosi'l Shelf Seas, W. 177-185. LcmdOlll.

HART, M. B .. & TARLING,· D .. H. 19'74. Cenomaruan paileQgeoglI"aphy iIn the Nocth Atlantic and potSSi'ble mid-Cenomanilllln euJStaJtic rnovemenJbs and theiJr lJm- plieatiO'lls. palaeogeogr. PaZaeoclimat. Palaeoecol., 15 (2), 95-108. Amsterdam.

HILBRECHT, H. 1986. On the oorrelaition of the U.~er Canomamdan and Lower 'DuronialIl. of ~d and Germany (BOIreal and N-Tretby;s). Newsl. Stratigr.,

15 (3), 115-138. Berliln - StlUttgaJrt. .

HUSS, F. 1962.. Distribution of planktonic and benthonic Foraminifera in the UjppeIl' Cretaceous sediments of NW Polaind. Acta Geol. Polon., 12 (I), 113-157.

~arsza~. .

JEFFER~~;R. P. S. 1963. The 'stratigOC"aphy of the Ac:tinocamax plenUiS Subzone (TUronian) in the Angl()-:Paa-is Basin. Proc. Geol. Assoc., 74 (1), 1-33. London.

JENKYNS, H. C. 1980. Cretaceous anotXic even1ls: i'.r0lI'll cOIIltilnentis to oceans. J. Geol.

S()C. LAndon, 137 (2)., 171-188. London.

- 11)85. The Early ToaJl"'cialll and CenOllIlallialn - Turoniwn oooxic events in EuIl"ope: oompall"isons and contll"aiSts. Geol. Rdsch., 74 (3), 505-518. S:t.utt.gaT!t.

KENNEDY,

W.

J. 0.1969. The correl'llltfun of the Lower Challk of _southeaist England . . Proc.- Geol. Assoc., 80(4), 459-560. LondOlll.

Mib-"CRETACEOUS EVENTS 73

KENNEDY, W. J. & GARRISON, R. E. 1975. Morphology ami genesis Of lIlOduila:r 'chalks 8iIld hardground5 in the Upper Cretru::eoUiS of southenn Eng181Il1d. Sedi- mentology, 22 (3), 311-386. Oxford.

MARCINOWSKI, R .. 19'14. The · k"an&g.re!SlSiv.e Cretaceous .. (U~ AIlbiaal through 'DUJrooian) deposits of the Po1d.sll J,UJra 9hain. Acta Geol. Polon., 24 (1), 117-217.

Wa:rISzawa. '

- 1980. Cenomaman ammanites from ~rIIl$J. Demooratic Republic, Poland, and the Soviet UniOlIl,. Acta Geol. Polon., 30 (3), 215-325. Warsza.wa..

MARCINOWSKI, R. & RADW ANSKI, A .. 1983. The mid-Cretaceous tmal;sg;ress:ion

onto the Central Poaish UplaindL'l (margilIlal part of the Centml EUJrqpean

,.,. :aas~n). Zi~teli4na, 10, 65-95. Mwchen. ,

MARCINOWSKI, :a.~ & WALASZCZYK,

i.

1985.M!id-Creiaceorwi; ·d€!p~ts 'arui bi-o-

,. ' .. st:ratiglraiphy of if;heAlriJnqpol seclion, CehWaIl POlilsh Uplands.OsteTTeichisc1ili

.·Akad. Wissemchaft. Sch'l'iftenTeihe deT Erdwissenschaitlischen;· Komissionellt,l

71:27-41. Wien.. . ... . . ' .

MARCLNOWSKI, R. & WIEDMANN, J. 1985. '.I1he A1b~a:mmOrid.te :hwna of Pollmd . 'mid . its lP8l1eqgeogr~hicaJ. s~fiai.nce. Acta Geol .Polon.,· 35(3-4), 199-219:

. War,gmwa.· . . . . ' .

Ml'LEWICZ,J .. 1959. Die. islt:ratiJgtraphi.sche Ednteillung der. Kreideablagell'ungender IIlOl'dsudetischen Mulde. Zt. Angewandte Geol., 5 (6), 261-2'63. Bedin.

- 1963. Die. faziellen Verhij[1lni,S'.Se ;in der NOIl',asudetischen Kreide. Ber~ Geol.

Ges . . DDR~ 8 (2), 130...;140. Bel"litn.. . .

POZARYSKI, W. 1947. A phOSlPhate depOsits oft-he north-eastern maa'lgID of the Holy Cr0S5 MountaLns. Biul. Inst; Geol., 27, 1,-5.6. WaIl'Szawa.

,1948. Jura:ssj.c ,and CreitaoceOlUS lbetlWeenRadom,. Zawich<l!St arid Krasnik Central Poland). Biul. Inst. Geol., 46, 3-141..WaIl'Is'zawa. '.

1956. KIl'eda. In: Regianallna Geo1ogia ~lski, rtom 2 (Region LubeLski) . [In ... Polish], pp. 14-62. P.W.N.; Krak:6w. .

RADWANSKI,.S. 1966. Upper CretaceOus facies 8iIld faJIma,g iln tlhe centll'al part of the Sudety Mts. Rocz. Pol •. Tow. Geol., 36 (2),99-119. Krak6w. · . . SAMSONOWICZ, J. 1925. Esquisse geruogique des env.iro:rls· de Rach.6w sur la

VistuUe et les tIl'am.sgression'S de l' A!lbien et au Cenomaonien ^diairu; le si1l1on

!l1ocd-europeen. Bull. Serv. Gliol. Pologne, 3 (1-2), 45-118. Warszawa.

- 1934. Ex.Plication de la feuiiJ.le Opa.t6w, WJ. 1-117. SeTv. Gliol. Pologne; WaT- szawa

SCHLANGER. S. O. & JENKYNS, H. C. 1976. Oretak:eoU5 oceamc anoxic everul!s:

causes ami ooru;eqU€!IlCe5. Geol. Mijnbouw, 55 (3-4), 179-184. Cu1embOll'g.

SEIBERTZ, E. 1979. StxaJt~hilSlch-fazielle En!t.wdoklUJng des T:u1l'OlIl iro siidOst:lisehen Mi1nstel'land (Oberk're1de. NW-DeUitlschaand). Newsl. StratigT., 8 (I), 3-60.

Berlin - Stuttgart

W ALASZCZYK, 1. 1984. Geol,ogy of the AIl!Ilopol 8iIllticlilIle Un PolilSlh}. Unpublished gTaduate paper, 1-72; Univemi.ty of WaIl'I'IIaw.

ZAPALOWICZ-BILAN, B. 1981. Foraminifem biofaClies of the Upper Cretaceou:s of· the Lubliln Coal Basin. Geologia, 7. (4), 5-37. WaIl',gzawa.

ZIEGLER, P .. A. 1982. Geo1ogica[ Atlais of Western arul. CentraJI. Europe, pp. 1-130.

Shell & ElsevieT; Amsterdam.

74 lRENE:t1S,ZW ALASZGZYK

l. WALASZGZYK

' .. :;

SRODKOWOKBEDQWE,NlECIĄGŁOSCJ . SEDYMENTACYJNE

W PROFILU ANNOPOLA NAD WISŁĄ_,

(Streszczenie)

,Praca przedstawia próbę interpretacji niecUmłościsedymen.tacyjnYch w środ­

Irowdkredowym profiliU Amlqpol<a naId Wlisłą (patrz fig. l). W skondetll9O\WillYCh utworach all'bu - do1I!1ego twrooo :wy1l'ÓŻIllić moZIna, 5 nieciągłości (patrz fig. 2--{ł

oraz ;pl. 1-2) po.clikIreślonych mptoWl[lą mnianą liitologdi (nieciągłości' 1-2) lUb wy- rażonych powierzchini:ami twardych den ze stowall'zysZOl!lymi lukami stmtygrafiici- nymi (nd.ecią.głośei 3 - 5). W

trze.cm

jpl'Zypadk8ch ,(nieciągłości l, 3 oraz 14) UJSt:Iill.ć można równie-! ich związek ze żmia!iltami głę'bolltości Zbiomika sedymemacyjlIlego

(patrz fig. 4). , " ,

Nieciągłości W p:ro!N'Il AIninopOla, z racji jego położenia w śraod:klQwej kredzd.e

na syn:sedymentącyJnie podnoszącej się stT:ukitJune (tzw. Próg W;isły hlb, Pil'bg Amloo- pola), przypisywane bYły <hiałaJlIlości tej iSbr~urY'. Ich dOlbra korellacja CZlllSOIWB zall:m.'loogLcZltlymiżjawdskami w ilOlIlY'Ch profilaCh Polski i Eur<llPY może śwliadczyć jedinalkże, iż !Są one l.dk.alnym Wytt'azem poWlSzeahillY'Ch, środllroWdklredowych wy- dW:r.reń. 'Dziala'lno,Ść Pil'ogu AmlopdJa, poprzez zwolnienie sedymentacji, była czyn- nikiem IŚ,przyjającym zapi.sCIWi tych wyduzeń, ja:k teżod,pow!iedziaInym za kpn- dein.sację osadów w dIi1.rterwałaJch poImiędzy po8Z1Crlególnymi nieciągłościami~