The Zechstein (Upper Permian) Main Dolomite deposits of the Leba ...

FACIES

14

151-200

Taf. 24-37

1 Tab.

10 Abb.

ERLANGEN 1986

The Zechstein (Upper Permian) Main Dolomite Deposits of the Leba Elevation, Northern Poland: Facies and Depositional History Hauptdolomit (Zechstein, Oberperm) in Nordpolen (Leba-Schwelle)" Fazies und Ablagerungsgeschichte

Tadeusz M. Peryt, Warszawa

SCHLUSSELWORTER:

SEDIMENTOLOGIE - KARBONATPLATTFORM - OOIDSANDE - DOLOMITE - POLEN ZECHSTEIN

-

OBERPERM

S U M M A R Y

or d e p o s i t i o n under a c o n s t a n t d e p t h of water.

The M a i n D o l o m i t e of the L e b a e l e v a t i o n

B e c a u s e of the d i f f e r e n t b e h a v i o u r

of the p l a t f o r m and the a d j o i n i n g basin,

is c h a r a c t e r i z e d by a b a s i n m a r g i n s e q u e n c e

the relief b e t w e e n t h e m was a c c e n t u a t e d

progressing shorewards

d u r i n g s e d i m e n t a t i o n and is e s t i m a t e d to

wackestones/mudstones sils,

from argillaceous c o n t a i n i n g w h o l e fos-

to p e l o i d a l and p e l o i d a l - b i o c l a s t i c

and lump d e p o s i t s

(possibly r e p r e s e n t i n g

l a g o o n a l facies),

to a f r i n g i n g o o l i t e flat

facies and a t i d a l - f l a t complex. cies sequence,

This fa-

d e p o s i t e d on a r e l a t i v e l y

u n i f o r m and gentle b a s i n slope,

indicates

h a v e b e e n 40 m at the end of the M a i n D o l o mite. The d e p o s i t i o n a l h i s t o r y of the M a i n D o l o m i t e on the Leba e l e v a t i o n i n d i c a t e s that s u b a e r i a l e x p o s u r e of the c a r b o n a t e platforms

in o t h e r areas was b r o u g h t a b o u t

that the area was a h o m o c l i n a l ramp w h i c h

by s y n d e p o s i t i o n a l

has m o d e r n c o u n t e r p a r t s

ated an o t h e r w i s e r e l a t i v e l y simple d e p o s i -

in the P e r s i a n

t i o n a l history.

Gulf and S h a r k Bay, A u s t r a l i a .

The d e p o s i t i o n a l h i s t o r y s u g g e s t s

tectonics which complic-

a

s h a l l o w i n g u p w a r d s s u c c e s s i o n on the car-

INTRODUCTION

b o n a t e p l a t f o r m area. S e d i m e n t a t i o n was locally i n t e r r u p t e d by s m a l l f l u c t u a t i o n s in sea level.

In contrast,

the a d j a c e n t

S e d i m e n t a t i o n in the Z e c h s t e i n b a s i n was c o n t r o l l e d by e u s t a t i c s e a - l e v e l changes

c e n t r a l p a r t of the P e r i - B a l t i c Gulf shows

(SMITH 1980, CLARK & T A L L B A C K A

1980, P E R Y T

a d e e p e n i n g u p w a r d s s u c c e s s i o n at the com-

et al.

m e n c e m e n t of the M a i n D o l o m i t e d e p o s i t i o n

d u r i n g the d e p o s i t i o n of the p r e - e v a p o r i t e

f o l l o w e d by e i t h e r a r e d u c e d d e e p e n i n g

Zechstein Limestone

Address;

Dr. T. Peryt,

I n s t y t u t Geologiczny,

1985). F l u c t u a t i o n s of s e a - l e v e l

led to p e r i o d i c

R a k o w i e c k a 4, P L - O O - 9 7 5 W a r s z a w a

sub-

152

aerial with

exposure

intense

sediments ted

meteoric

(PERYT

that

the

three

The

were such

a shallowing-upwards

second

unit

Zechstein

glacioeusta-

as a w h o l e

facies

the M a i n

(= H a u p t d o l o m i t ) ,

also e x h i b i t s

ing-upward

sequence

paltform POWSKI

areas

et al.

& TALLBACKA 1984).

deposits

(CLARK

been

1980,

PISKE

of Main

subject

1978, PISKE

Dolomite a shallow-

et al. CLARK

1978, 1980,

PERYT

also

1985b),

et al.

& SCHRETZENMAYR

however,

deposition

to c o n t r o v e r s y

(DEPOWSKI

1978,

PISKE

CLARK

1984).

their different

several

it has

subcycles

in the M a i n

been

ed by

can be r e c o g n i z e d ,

no e v i d e n c e

rise.

formed

(FUCHTBAUER NEMANN

PISKE

distinguished subcycles.

et al.

Conventional base

slightly

inclined

et al.

ely

merged

and

posits

formed.

A fall

to be some

7Om

ated

formed

large,

MAYR

(1984).

that

if the same

of the e n t i r e

gression

is i n d i c a t e d

subaerial

environment

did not p r e s e n t

the

to the e a s t e r n

two w e l l s

this

would

position.

a difference

ated a r e l a t i v e l y the b a s e

further

that the

only

tenuous

from the p l a t f o r m

considering

Amsterdam

sub-

The d i f f e r e n c e s

de-

partly

due

(estim-

tation

caused by

in the

platform.

Such

by d i s s o l u t i o n

a rein a

the authors data),

b re c -

ficult

to estimate.

paleotectonic which offers

form was

completely

lowed by a r e g r e s s i o n fall of some Main

Dolomite

9Om, according

flooded,

70 m w h i c h

marked

deposition.

the p l a t -

and w a s

indicating

coring

is (no core

in E m m e n - N i e u w Fig.

2).

fol-

a sea-level

the end of

a unique

during

elevation

the

Dolomite

disturbances a key

and

as to

fluctuations

of the M a i n D o l o m i t e

in the basin.

diffi-

platform

to study

of the M a i n

of the s e a - l e v e l

deposition

1980:Fig.

of its s t a b l e

the L e b a

the s t u d y may p r o v i d e

the e x t e n t

where

Because

tectonic

tec-

are s o m e t i m e s

opportunity

history

are

of s e d i m e n -

& TALLBACKA

position,

with negligable hence

rates

is p a r t of the P r e c a m b r i a n

depositional

1984),

1OO m,

synformational

(CLARK

subcycle

(after

local

of w h i c h

the e f f e c t s

During

& SCHRETZENMAYR,

the b a s i n

as

in i n t e r p r e t a t i o n

24)

crusts.

to PI S K E

1980:

shal-

at 60-80 m depth.

the poor

tonic m o v e m e n t s

of c a r b o a n t e

of some

that

for this m o d e l

to d i f f e r e n t i a l

and the f o r m a t i o n

in s e a - l e v e l

platform

during

ciation

a rise

postul-

by other wor-

as s h a l l o w

deposits

I - CLARK

To r e m o v e

at a m u c h

of the s l o p e

kink in

24 in-

model

suggested

the e v i d e n c e

(1984)

sabkha

(however,

the b a s e

However,

2 and

50 m.

interpreted

slight.

resulted

analytical

with

applied

50 m in ver-

flat e v a p o r i t e

have b e e n

than

was

a difference

CLARK's

of the s l o p e

CLARK

depth

& SCHRETZEN-

a peculiar

of only

anomaly

(SANNEthat

the same beds

He e s t i m a t e d

the

considered

d i f f e r by some

could

in the

area

and

that

flat and

to be r e l a t i v -

150 m, b u t his Figs.

apparent

with

had

SAN-

1985).

implying

by P I S K E

Drenthe

1977,

assume was

(1980:154)

w o u l d be i n t r o d u c e d

Dolomite

& PERYT

interpretation

floor

areas w e r e not

the s e c o n d

CLARK

control-

the b a s i n

6),

of s e a - l e v e l

as a s s u m e d

kers.

in s e a - l e v e l

exposure

Fig.

found

islands w h e r e

)

towards

1978:

initiat-

he

to their model,

some

cross-sections

each

two t r a n s g r e s s i v e - r e g r e s s i v e

subcycle

DEPOWSKI

platform

cycle

& BOLZ

of the L o w e r A n h y d r i t e

MANN

It has

of the M a i n

SCHLAGER

1978,

from

to the g e o m e t r y

the e v a p o r i t e

lower

& SCHRETZENMAYR

According

first

1964,

and

resulted

the W e r r a

four s e p a r a t e

he c o n c l u d e d was

(1980:

that

during

(1980)

platform.

led the s e d i m e n t a t i o n

dicate

to

CLARK

exposure

of the p l a t f o r m

Conve r s e l y ,

that

related

Because

of s u b a e r i a l

carbonates,

exposure

the

that at least

a sea-level

s lope

sequence

of the sea-levels

suggested

subcycles

suggested,

approaches

recognized

tical

can be d i s t i n g u i s h e d w i t h -

Dolomite

fluctuations 161)

been

(1984)

of the W e r r a e v a p o r i t e

which

of s e a - l e v e l

by C L A R K

& SCHRETZENMAYR

of a b o u t Recently

in the scale

as s u g g e s t e d

fluctuations

feature

to s u b a e r i a l

Dolomite

SANNEMANN

DECLARK

& SCHRETZENMAYR

subjected

1980,

the

in the c a r b o n a t e

plLatform areas

the c o n t r o l s

et al.

1981,

which were

exposuxe

have

(SANNE~ANN 197~,

1980,

These

sequence.

of the S t a s s f u r t ,

cycle,

facies

sugges-

fluctuations

which

The d i f f e r e n c e s changes

to d e v e l o p w i t h i n

Limestone

carbonate

of the

It has b e e n

three

subcycles

Zechstein

shows

1984).

and

platforms

diagenesis

the f l u c t u a t i o n s

tic in origin, caused

of the c a r b o n a t e

el s e -

153

Fig. I. A r e a studied, i n d i c a t i n g the l o c a t i o n of the b o r e h o l e s and the t h i c k n e s s of the M a i n D o l o m i t e s e q u e n c e in N o r t h e r n Poland. I n s e r t map: T-T Line = T e i s s e y r e - T o r n q u i s t Line.

154

GEOLOGICAL

sition of the Z e c h s t e i n L i m e s t o n e

SETTING

was p a r t of the b a s i n a l In the area of the Leba e l e v a t i o n

the

zone

the area

(DEPOWSKI

1978)

and only later d u r i n g d e p o s i t i o n of the

Main D o l o m i t e s u c c e s s i o n has b e c o m e known

Lower Anhydrite, was

during exploration

tiated so that the d e p o s i t i o n of the O l d e s t

for the p o t a s s i u m an@

rock salt d e p o s i t s of the W e r r a cycle. about

100 wells,

study

(Figs.

From

53 were s e l e c t e d for the

I, 2) i n c l u d i n g all w e l l s w i t h

full core recovery.

P r e v i o u s w o r k has shown

~hat the M a i n D o l o m i t e

forms a l e n t i c u l a r

b e l t r u n n i n g along the e a s t e r n Central P o m e r a n i a n Peninsula,

flank of the a paleogeo-

graphic h i g h d u r i n g the Zechstein, the m i c r o f a c i e s

to p r o b a b l e s u p r a t i d a l c o n d i t i o n s end of d e p o s i t i o n

H a l i t e took p l a c e in a m o r p h o l o g i c a l l y d i v e r s i f i e d basin.

leading at the

(PIATKOWSKI in D E P O W S K I

1978).

anhydrite,

so it seems that at the end of

the O l d e s t H a l i t e was s m o o t h again

deposition

the r e l i e f

(PERYT et al.

1985).

S a n d w i c h e d b e t w e e n the O l d e s t H a l i t e and M a i n D o l o m i t e occurs The s u l p h a t e s

the Z e c h s t e i n

over an a l m o s t flat sur-

the Upper A n h y d r i t e .

(mainly anhydrites)

consist

of i n t e r b e d d e d c o n g l o m e r a t i c and r e c r y s t a l lized a n h y d r i t e s

In the Leba e l e v a t i o n area,

areas of m a x i -

of the e a r l i e r m i n i m u m d e p o s i t i o n of the

anhydrite nodules

sea t r a n s g r e s s e d

However,

m u m d e p o s i t i o n of salt c o i n c i d e w i t h areas

and that

s e q u e n c e is r e g r e s s i v e due

to gradual s h a l l o w i n g of the area,

the relief d i f f e r n -

beds

and m u d r o c k s w i t h m m - s i z e d and o c c a s i o n a l d o l o m i t e

(PERYT 1986), w h i c h s e e m to have orig-

i n a t e d in s h a l l o w salinas.

At the end of

face formed by U p p e r S i l u r i a n siltstones,

Upper Anhydrite sedimentation

subordinate

d r e w and the u p p e r m o s t p a r t of the U p p e r

Rotliegendes

limestones,

and,

conglomerates.

Fig. 2. The P u c k Bay area; 3, 5, 6, 7, and 8.

locally,

thin

During depo-

the sea w i t h -

Anhydrite underwent brecciation

l o c a t i o n of the b o r e h o l e s

and gyp-

and of the areas shown in the F i g u r e s

155

sification

(PERYT et al.

1985).

the B u n t s a n d s t e i n

i n t e r b e d d e d s u l p h a t e and

c a r b o n a t e d e p o s i t s occur. In the P u c k Bay area, dolomites

the thickness

and limestones c o n s t i t u t i n g

M a i n D o l o m i t e varies

of the

from 6.5 m in the SE

are a c c o m p a n i e d

(Fig.

stein b a s i n

The t h i c k n e s s p a t t e r n is very r e g u l a r

carbonate

I). The Main D o l o m i t e d e p o s i t s

are over-

In the K o p a -

lino region, one such s e q u e n c e is 24 m thick

part of the region to 49.0 m in the north. (Fig.

In p l a c e s they

by m u d s t o n e s .

5). In other parts of the Zech(e.g., in w e s t e r n Poland),

the

facies passes s h o r e w a r d g r a d u a l l y

into a s u l p h a t e

facies;

the t r a n s i t i o n

lain by the B a s a l A n h y d r i t e or - in the

b e i n g related to a m u d - f l a t sequence, w i t h

n o r t h e r n p a r t of the area - by the P l a t y

mudstones,

Dolomite, cycle:

b e l o n g i n g to the n e x t e v a p o r i t e

PZ 3. A d i s t i n c t i v e s h i f t of the

stromatolites

ular anhydrites.

The s e q u e n c e appears to

be s i m i l a r to that o b s e r v e d in the R e c e n t

two facies belts exists b e t w e e n

the Platy

P e r s i a n Gulf sabkhas

D o l o m i t e and the M a i n Dolomite.

Both car-

in K o p a l i n o

b o n a t e units by their

can be e a s i l y d i s t i n g u i s h e d

log c h a r a c t e r i s t i c s

lithology.

and their

and d o m i n a n t nod-

(SHINN 1983). However,

the s i t u a t i o n

is different:

A c c u m u l a t i o n s of f i n e - g r a i n e d w e l l

sorted

ooid sands s e e m to r e p r e s e n t b a r r i e r

The P l a t y D o l o m i t e is c o v e r e d

islands

w h i c h w e r e only s e l d o m s u b a e r i a l l y exposed,

in the s o u t h e r n p a r t of the area s t u d i e d

and - d i s r e g a r d i n g the c l e a r l y r e p l a c i v e

by the M a i n A n h y d r i t e ,

n a t u r e of the a n h y d r i t e s

it of the Z e c h s t e i n elevation

area.

the u p p e r m o s t d e p o s -

sequence

in the L e b a

The P e r m i a n s u c c e s s i o n is

c a p p e d by the T r i a s s i c B u n t s a n d s t e i n . lower B u n t s a n d s t e i n and mud deposits, supratidal RYT

The

is r e p r e s e n t e d by sand

i n d i c a t i n g i n t e r t i d a l and

environments

(CZAPOWSKI

& PE-

1984).

the change from ooid g r a i n s t o n e s

24/6)

-

to s u l p h a t e

cannot be e x p l a i n e d as a simple facies succession.

Instead,

the s u l p h a t e facies can

be p r e d i c t e d to occur s h o r e w a r d s

some dis-

tance from the o o l i t i c a c c u m u l a t i o n s ,

i.e.

in the L e b a region w h e r e such shore line c o m p l e x e s h a v e b e e n recorded. tailed d i s c u s s i o n thereof

In the w e s t e r n p a r t of the area, b e l o w

(Plate

Chapter:

A m o r e de-

w i l l be given in

D e p o s i t i o n a l Sequence.

Fig. 3. T h e i r r e g u l a r l i m e s t o n e d i s t r i b u t i o n in the M a i n D o l o m i t e s e q u e n c e (notice the l i m e s t o n e s are r e l a t e d to the u p p e r p a r t of the M a i n Dolomite). The w e l l s s h o w n are not l o c a t e d along a s t r a i g h t line; the d i s t a n c e b e t w e e n the end w e l l s is 12.6 km.

156

F i g . 4. L i t h o f a c i e s sequence in w e l l s l o c a t e d in t h e e n v i r o n s of Leba. The wells are not located along a straight line; the distance between t h e e n d w e l l s is 6.2 km. P h a s e s o f the Main Dolomite deposition correspond to those presented in F i g . 9.

Facies

Texture

Major components

Biota

Photos

Depositional environment (SMF/FZ)

Remarks

peloidal

W & P

peloids; quartz grains

rare bivalves and ostracods

PI. 24/I,2

23/8, 9

association: unfossiliferous M, peloidal W, laminoids

peloidal

P

peloids; bioclasts

abundant: biP1. 25/1-5 valves, brachiopods, gastropods, ostracods, foraminifers, dasycladaceans

8-10/2, 7

often layers with one group of fauna

peioidalbioclastic

G & P

peloids; bioclasts; ooids; rare lumps and intraclasts

abundant: bivalves, brachiopods, gastropods, foraminifers, serpulids

P1. P1. P1. PI. PI.

24/3 26/1-4 27/i-3 28/i-5 29/1-3

12/6

biota: bioclasts or whole shells. Association: microbial deposits, occasionally ooidal-bioclastic G

oolitic

G (& rare P)

ooids; occasio- sparse: bivalves, nally bioclasts, encrusting peloids, lumps foraminifers and vadoids

"PI. PI. P1. PI.

30/1-5 35/2 36/1,2 37/4,5

15/6

vadolitic

G (rare P)

vadoids; ooids; peloids; lumps

sparse, mainly bivalves

PI. 36/3,4 P1. 37/1,3

microbial

B

peloids; bioclasts

encrusting foraminifera, bivalves

P1. 32/3 P1. 33/1-3 P1. 34/I-5

19 & 21/8

lump

P & G

lumps; intrasparse: biclasts; peloids; valves, ostracods, rare dasycladaceans

PI. 31/I-3 PI. 32/I-2

1717,8

muddy

M & W

peloids

rare

T a b . I. C h a r a c t e r i s t i c s of the lithofacies thern Poland. Abbreviations: B -Boundstone, W - Wackestone. SMF - Standard Microfacies SON 1975).

--

23/8,9

stromatolites are often accompanied by peloidal-bioclastic P & G and occasionally by oolitic G; laminoids are accompanied by peloidal P

association; peloidal W & P; commonly laminated with terri8enous clay material

of the Main Dolomite, Leba elevation area, NorG - Grainstone, M - Mudstone, P - Packstone, Types, FZ - Standard Facies Zones ( after WIL-

157

W

15.0km

4

KOPALINO IG1

A

Q

A9 |A

o

19.7km

~

~4km

SALINO IG1

~Okm----.-,,

WIDOWO ONZ1

D~aKI IG1

E

SLAWOSZYNKO ONZl

A I A

lil[1

X

X X

*

2

X X

1 )[

W

P P

G G

o

ililtl

G E>

_a561.6- P A-lgR -

L

m-~- TT1 X

X 9

o

/ I~

X X

X X

G

Alg

Fig. 5. L i t h o f a c i e s s e q u e n c e in the w e l l s located b e t w e e n K o p a l i n o and S l a w o s z y n k o (see Figs. I and 2 for location. The w e l l s are not lying along a s t r a i g h t line; the d i s t a n c e b e t w e e n the end w e l l s is 23.0 km . For e x p l a n a t i o n see Fig. 4.

The rocks of the M a i n D o l o m i t e the name says m a i n l y dolomites.

_lOm

are as

Limestones

o c c u r in a b e l t r u n n i n g a p p r o x i m a t e l y p a r a l lel to the p r e s e n t extent of the B a s a l Anhydrite

(Fig.

I), and w e r e also r e c o r d e d

in the n o r t h - w e s t e r n p a r t of the Puck Bay area

(Fig. 2) near Debki and W i d o w o

other isolated wells

(e.g., Opalino~

of the Lake Zarnowieckie, see Fig. 840.1

limestones origin

south

3).The

are p e r s u m e d to be of s e c o n d a r y

(Plates 24/3-5;

carbonates

and

35/2-4;

37/2). The

are a c c o m p a n i e d by sulphates.

The c o n t e n t of a n h y d r i t e is a b o u t

1%

in

the s o u t h e r n region and about s e v e r a l p e r cents in the n o r t h e r n region. of these rocks ranges

The c o l o u r

f r o m p a l e grey and

158

beige Main

in the Dolomite

m o s t parts southern black mite

thickest

and in the

of the Main

Puck

Bay area

in the m i d d l e deposition

area w h e r e

development

marly

lower-

Dolomite to dark

p a r t of the

in the s o u t h e r n intercalations

of the

exhibit

a distinct

and upper-

ation

in the

clusions

grey

and

ison

(Figs.

of each

Main Dolo-

counterpart:

Puck

history

Bay

2,

which

areal

4-8).

Therefore,

can be d e r i v e d

lithofacies

to its

to r e c o n s t r u c t the

LITHOFACIES

a very

Dolomite

of the L e b a

elevation

recent

of d e p o s i t i o n .

lithofacies

It may be s u b d i v i d e d

lithofacies

the con-

from c o m p a r -

may be used

and a b i o t a - r i c h

common

zon-

are common. Peloidal

The m o s t

and v e r t i c a l

in the M a i n

I).

(Table

stones

I)

sparse

into a b i o t a - p o o r

facies.

low-diverse

The p r e d o m i n a n t

The

fauna

textures

and p a c k s t o n e s ,

first

with

contains

(Plate

24/

are w a c k e very

small

Fig. 6. L i t h o f a c i e s s e q u e n c e in w e l l s l o c a t e d b e t w e e n S u l i c i c e and C h l a p o w o (see Fig. 2 for location). The w e l l s are not lying a l o n g a s t r a i g h t line; the d i s t a n c e b e t w e e n the end w e l l s is 11.3 km. For e x p l a n a t i o n see Fig. 4.

159

peloids

(average 0.2-0.4 mm),

a l t h o u g h oc-

c a s i o n a l l y m u c h b i g g e r s p e l o i d s occur. T h e r e are s e v e r a l p o s s i b l e o r i g i n s these p e l o i d s

for

(see s u m m a r y by F L U G E L

1982:

are a s s o c i a t e d w i t h u n f o s s i l i f e r o u s mudstones.

An absence of a fauna w o u l d be ex-

spected if s a l i n i t y was during transgression

131-136) b u t a fecal p e l l e t o r i g i n seems

w i t h r e s i d u a l brines,

to be m o s t likely b e c a u s e the o c c a s i o n a l

SMITH

bioclasts

mite deposition.

are of c o n s i d e r a b l y g r e a t e r size

(Plate 24/2)

as s u g g e s t e d by

and at the end of M a i n Dolo-

and no ooids have b e e n iden-

tified in this or the a d j o i n i n g Accordingly,

1980:29)

lithofacies.

b o t h grain types may be ex-

c l u d e d as p o t e n t i a l p r e c u r s o r s

of peloids.

The b i o t a - r i c h p e l o i d a l a whole contains

w e s t of Andros

Island,

peloidal wackestones

and p a c k s t o n e s

are r e l a t e d to a s h a l l o w

s u b t i d a l e n v i r o n m e n t of m i n i m u m w a t e r energy and i n c r e a s e d s a l i n i t y

(ILLING 1954,

1974). A s i m i l a r e n v i r o n m e n t is envi-

lithofacies

as

a relatively diversified

faunal a s s e m b l a g e w h i c h seems n o r m a l m a r i n e salinity.

In the r e g i o n of the G r e a t B a h a m a Banks,

ENOS

locally i n c r e a s e d

(because of m i x i n g

to i n d i c a t e

However,

commonly

i n d i v i d a u l beds c o n t a i n a r e s t r i c t e d fauna, e.g., o s t r a c o d s

or foraminifers.

The fauna

is a c c o m p a n i e d by p o o r l y p r e s e r v e d a n d uni d e n t i f i a b l e moulds of d a s y o l a d a c e a n s 25/I,4,5).

Peloids

(Plate

are u s u a l l y g r e a t e r than

in the b i o t a - p o o r p e l o i d a l

lithofaoies,

and

saged for the Main D o l o m i t e lithofacies.

are c h a r a c t e r i z e d by g e n e r a l l y g r e a t e r var-

The p e l o i d a l

iations in size;

l i t h o f a c i e s w a s r e c o r d e d in

the NW part of the area studied, Leba region, w h e r e

it

in the

is a s s o c i a t e d w i t h

unfossiliferous mudstones which probably also o r i g i n a t e d environment.

in a s u b a q u e o u s h y p e r s a l i n e

It also occurs at the b a s e of

the M a i n D o l o m i t e

in the S w a r z e w o - Z d r a d a

area and at the top of m a n y wells

(but n o t all)

located to the south of Zdrada,

where peloidal wackestones

and m u d s t o n e s

stone

the m a i n texture

(Plate 25/I-5).

ritized bioclasts

is pack-

Some p e l o i d s

are m i c -

as i n d i c a t e d by the pre-

sence of r e c o g n i z a b l e

foraminifers

(Plate

25/3). The m i c r i t i z a t i o n of b i o c l a s t s

is

characteristic

of m o d e r n r e s t r i c t e d sub-

tidal s e t t i n g s

(ENOS 1983:279)

and the same

are a s s u m e d for the

environment

conditions

in w h i c h the b i o t a - r i c h p e l o i d a l originated.

lithofacies

The l i t h o f a c i e s c o m m o n l y occurs

Fig. 7. L i t h o f a c i e s s e q u e n c e in w e l l s located b e t w e e n Zdrada and S w a r z e w o (see Fig. 2 for location). The w e l l s are not lying a l o n g a s t r a i g h t line; the d i s t a n c e b e t w e e n the end w e l l s is 8.7 km. For e x p l a n a t i o n see Fig. 4.

160

in the c e n t r a l p a r t of the M a i n D o l o m i t e

The p r e d o m i n a t

sequence

stone,

in the s o u t h e r n part of the area

studied.

common.

Grainstones

sometimes Peloidal-bioclastic This

lithofacies

texture is that of a grain-

but in some s e c t i o n s p a c k s t o n e s and p a c k s t o n e s

are

a c c o m p a n i e d by s t r o m a t o l i t e s ,

lithofacies

minoids,

is c o m p o s e d of peloids

tries have been r e c o r d e d

w h i c h vary in size but are u s u a l l y 0.5 mm

are

la-

and o c c a s i o n a l l y m i c r o b i a l tapes(Plate 26/I).

o r i g i n of some e x t e n s i v e l y

The

recrystallized

in d i a m e t e r and b i o c l a s t s w h i c h o c c a s i o n a l -

laminated cavity-fill

ly are a c c o m p a n i e d by ooids

u n c e r t a i n but it may r e p r e s e n t s u b m a r i n e

2; 27/1,3).

The b i o c l a s t s

(Plates 24/3; 29/I-3)

bivalves,

serpulids, serial,

28/2-5)

c o n s i s t of w h o l e

or f r a g m e n t e d

brachiopods,

ostracods

spiral

(Plates 26/I,

(Plates

gastropods,

and f o r a m i n i f e r s

and encrusting).

(uni-

In some

cases f r a g m e n t s of algal stems have been

(Plate 27/1,2)

is

c e m e n t as i n d i c a t e d by the o c c a s i o n a l occurrence of f o r a m i n i f e r a c u r r e n c e of p e l o i d s

and the f r e q u e n t oc-

and b i o c l a s t s

incorpor-

ated in the f r a m e w o r k of the laminations; this

latter feature was not o b s e r v e d

accompanying stromatolites

in the

(Plate 32/3).

r e c o r d e d w h i c h may r e p r e s e n t Mizzia sp..

Fig. 8. L i t h o f a c i e s s e q u e n c e in w e l l s located in the s o u t h e r n p a r t of the area steadied. The w e l l s are not lying along a s t r a i g h t line; the d i s t a n c e b e t w e e n the end w e l l s is 67 km. For e x p l a n a t i o n see Fig. 4.

161

d e s c r i b e d by CLARK D r e n t h e area.

(1980:137) in the e a s t e r n

CLARK

assumed that the cements

formed under v a d o s e conditions,

layers w h i c h are rich in b i o c l a s t s

w h e n bio-

c l a s t i c m a t e r i a l was d e p o s i t e d

in supra-

In recent d e p o s i t i o n a l e n v i r o n m e n t s

tidal b e a c h ridges d u r i n g storms and then

grainstones

rapidly

tidal

lithified.

A recent a n a l o g was de-

s c r i b e d by P U R S E R & L O R E A U P e r s i a n Gulf beaches.

(1973)

some peloids

from the

The p r e s e n c e of al-

t e r n a t i n g m i c r i t e and sparite

laminae on

and the i r r e g u l a r p a t t e r n of

1984). The

lithofacies.

compaction

SER

by PUR-

(1980) w o u l d also s u p p o r t this c o n c l u -

sion.

The c a v i t i e s w h i c h have been s e c o n d a r -

ily filled by s u b m a r i n e cements,

could

The

lack of w i d e s p r e a d m a r i n e

of some ooids

particularly characteristic,

to have

formed in a lagoonal,

near-

-beach p o s i t i o n w h e r e

grainstones

whilst

formed in the c e n t r a l

the p a c k s t o n e s

parts of the lagoon.

occur

The b r o k e n

o f t e n coated by

Such

into

lumps are,

rare in c o n t r a s t to the o o l i t i c

grainstone (CLARK

later i n c o r p o r a t e d

(Plate 30/4).

l i t h o f a c i e s of eastern D r e n t h e

1980:133)

intraclasts

The l i t h o f a c i e s was

and only b e a c h

(PURSER & L O R E ~ J

however,

preted

is

laminae of c o n i a t o l i t e

deposits

the

1985a)

f r a g m e n t s of b e a c h r o c k ,

1973) nature, w e r e

is inter-

(PERYT

ridge ooids have been cemented.

ooid sands

lithofacies

conditions

as e v i d e n c e d by the p h y s i c a l

zone as o b s e r v e d in recent and a n c i e n t tidal (PURSER 1975). A c c o r d i n g l y ,

(beach

1979, P I E R S O N

for the Main D o l o m i t e o o l i t i c

have o r i g i n a t e d by b i o e r o s i o n in the tidal

peloidal-bioclastic

(HARRIS

same e n v i r o n m e n t a l

may be a s s u m e d

e n v i r o n m e n t w h e r e only a p a r t i a l s a t u r a t i o n The o b s e r v a t i o n s

to s u p r a t i d a l

environments

cementation

ooid

usually o c c u r in s h a l l o w sub-

(active shoals)

ridges)

c e m e n t a t i o n w o u l d be e x p e c t e d in a b e a c h

w i t h w a t e r occurs.

and

peloids.

and of w e s t e r n P o l a n d w h e r e

are c o m m o n

n o r t h e r n Poland,

(PERYT

the o o l i t i c

1985b).

In

lithofacies

occurs in the n o r t h e r n p a r t of the area

r e c o r d e d in the lower part of the M a i n D o l o -

s t u d i e d and in the M i l o s z e w o ONZI w e l l

mite in the S w a r z e w o - Z d r a d a

ated in the south and is a c c o m p a n i e d by

Fuck Day area)

and in

area

Debki

(southern

(western P u c k

loc-

l a m i n o i d a l deposits.

Bay area). Vadolitic Oolitic

lithofacies

The o o l i t i c

lithofacies

In the M a i n D o l o m i t e Of n o r t h e r n P o l a n d

lithofacies

is c o m p o s e d of

and in o t h e r parts

of the Z e c h s t e i n b a s i n

ooid g r a i n s t o n e s w h i c h are rarely accom-

a

p a n i e d by o o i d - b i o c l a s t i c

(Plate 37/1,3) w h i c h

is c h a r a c t e r i z e d by

alternating micritic

and s p a r i t i c laminae.

The grains g e n e r a l l y

are oval in shape and

packstones

grainstones

(Plates 30/1,2;

36/2;

Ooids are u s u a l l y w e l l - s o r t e d ,

and

37/4,5).

and their

size t y p i c a l l y v a r i e s b e t w e e n 0.2 and 0.7 mm.

The n u c l e i are b i o c l a s t s

p a r t i c u l a r type of coated grains occurs

show some p r o t u b e r a n c e s .

or peloids.

V e r y often the c e n t r a l parts of the ooids

QUESTER

(1964:465)

c o m p a r e d those coated

have b e e n d i s s o v e d or have b e e n i n t e n s e l y

grains w i t h the T e r t i a r y

recrystallized.

limestones

Some ooids s u f f e r e d p h y s i c a l

c o m p a c t i o n after i s o p a c h o u s tation took place 1985a),

c a r b o n a t e cemen-

(Plate 30/3,5;

PERYT

of ooid centres.

This s u g g e s t s

compacted

formed d u r i n g burial.

fabric

d e g r e e of c o m p a c t i o n varies individual sections grainstones

that the The

Ooid

are o f t e n m a s s i v e but in some

cases p l a n a r

(Plate 30/1)

or c r o s s - b e d d e d

(as in the u p p e r p a r t of the D e b k i IGI well). Ooids s o m e t i m e s o c c u r w i t h b i o c l a s t s ly bivalves),

peloids,

(main-

and lumps. V a d o i d s

are g e n e r a l l y s u b o r d i n a t e

except

the algal crusts was of inorganic,

c h e m i c a l origin.

The c o n c e p t of an algal

o r i g i n was also a c c e p t e d by F U C H T B A U E R

t h r o u g h o u t the

(Plate 36/I-4).

He i n f e r r e d that the c a r b o n a t e o c c u r r i n g between

and also after p a r t i a l d i s s o l u t i o n

Lithothamnium

and saw c e r t a i n s i m i l a r i t i e s .

in some

(1964:491)

a l t h o u g h he had p r e v i o u s l y re-

g a r d e d them as ooids. 42, PI.

3, Fig.

S A N N E M A N N et al

2) i n t e r p r e t e d

(1978:

the same

grains as ooids a s s o c i a t e d w i t h oncoids,

the

latter d i f f e r i n g only in their irregular, c a u l i f l o w e r shape, but not in size.

There

is a t r a n s i t i o n b e t w e e n the two types of grains.

CLARK

"pisoliths

(1980:141)

suggested

that the

formed d u r i n g the early d i a g e n e s i s

162

of the host s e d i m e n t by p r e c i p i t a t i o n laminated coatings b u r i e d grains".

of

around groups of already

According

to him,

perfect-

ly fitted contacts b e t w e e n the larger, regularly-shaped that

grains

However,

1985b) b e c a u s e

(PERYT

with

are c o m m o n l y a s s o c i a t e d

the p e l o i d - b i o c l a s t i c

bodies.

A very c h a r a c t e r i s t i c

the s u b t i d a l s t r o m a t o l i t e s

aneous w i t h the d e p o s i t i o n

Limestone

and lump for-

Those grains w h i c h are c a l l e d (PERYT 1983a,

1985b)

feature is a

(PERYT 1981),

in the Z e c h s t e i n

in w h i c h

laminae

of e n c r u s t i n g f o r a m i n i f e r a c o m m o n l y occur,

originated

in a b e a c h e n v i r o n m e n t w h e r e p e r i o d s

in

and

d e n s e type of l a m i n a t i o n s i m i l a r to that of

their f o r m a t i o n m u s t have been c o n t e m p o r -

"vadoids"

lithofacies

the lower part of the Main Dolomite,

they form thin i n t e r c a l a t i o n s or c o m p o u n d

the grains o c c u r inside lumps

and in the nuclei of other grains so that

mation.

are

gradational.

Stromatolites

i n - s i t u growth of

such grains has b e e n q u e s t i o n e d

lower and upper b o u n d a r i e s w h i l s t

in the l a m i n o i d rocks the b o u n d a r i e s

ir-

clearly showed

these could only have r e s u l t e d from

in situ growth.

defined

of

and e n c r u s t i n g f o r a m i n i f e r a may f o r m interlayers

(Plate 32/4).

This type of s t r o m a t o -

c e m e n t a t i o n a l t e r n a t e d w i t h those of trans-

lite o r i g i n a t e d

portation

and is c o n f i n e d to the S w a r z e w o - Z d r a d a - K l a -

r e s u l t i n g in the f o r m a t i o n of

c o m p o s i t e grains.

Vadoids were sometimes

t r a n s p o r t e d to the a d j a c e n t

lagoons,

e v i d e n c e d by the p r e s e n c e of v a d o i d in the p e l o i d a l deposits. (Plate 30/4)

as laminae

In one section

some vadoids s e e m to be auto-

chthonous.

n i n o belt.

Another

accompanies 34/5):

the l a m i n a t i o n

no f o r a m i n i f e r a l

zompaction which eventually

underwent

r e s u l t e d in a

lithofacies

is p o o r l y d e v e l o p e d ,

framework.

into the

This type, w h i c h

to the laminoid, was

in the Czarny Mlyn area)

(Plate

laminae w e r e r e c o r d e d and

peloids are c o m m o n l y i n c o r p o r a t e d

is a t r a n s i t i o n the v a d o i d s

type of s t r o m a t o l i t e

the p e l o i d a l

stromatolitic

Like the ooids,

in s u b t i d a l e n v i r o n m e n t s

area

found

(Central Puck Bay

and like the laminoids

they also prob-

~abric c o n s i s t i n g of very e l o n g a t e d grains

ably o r i g i n a t e d

(Plate 36/4).

it is d i f f i c u l t

In the L e b a region,

texture

ized by an a s s o c i a t i o n w i t h s u l p h a t e o c c u r

Accordingly,

to infer w h a t the o r i g i n a l

~r

in a s u b t i d a l environment. stromatolites

character-

and are i n f e r r e d to have formed in a h y p e r A r e c e n t a n a l o g of the e n v i r o n m e n t which vadoids

& KINSMAN

(PURSER & L O R E A U 1973,

1974),

although vadose

c o m p a c t i o n has not b e e n d e s c r i b e d , ably b e c a u s e extensively

saline environment.

are forming are the sabkhas

of the P e r s i a n Gulf SCHOLLE

in

prob-

the d e p o s i t s h a v e not b e e n flushed with freshwater

1980:142). The v a d o l i t i c

(CLARK

lithofacies occurs

L a m i n o i d rocks are u s u a l l y a s s o c i a t e d with peloidal

wackestones

and s o m e t i m e s w i t h often

form

and p a c k s t o n e s ,

lump grainstones.

They

mm-sized

intercalations which

r e p e a t in m i l l i m e t e r

to c e n t i m e t e r inter-

vals or e v e n t u a l l y f o r m c o m p l e x e s w h i c h are

in the n o r t h e r n r e g i o n of the D e b k i area

s e v e r a l tens of c e n t i m e t e r s

and in the M i l o s z e w o ONZI w e l l

u p p e r p a r t of the Main D o l o m i t e

in the Darz-

lubie IGI s e c t i o n

They are

south.

V a d o i d grains

peloid-bioclastic

in the far

also o c c u r in the

grainstones

of the c e n -

tral area.

(Plate 34/I).

generally unfossiliferous, bioclasts

This

lithofacies

litic b o u n d s t o n e s

Parallel

ostracods,

of s t r o m a t o -

(Plates 32/3;

(Plates 33/I-3;

34/3,5) and 34/2,4) w h i c h

very rare f e n e s t r a l

and

lamination,

c a s i o n a l small c u t - a n d - f i l l s t r u c t u r e s

lithofacies consists

l a m i n o i d rocks

but w h e n p r e s e n t

comprise bivalves,

rare f o r a m i n i f e r s . Microbial

thick as in the

ocand

fabric w e r e the only

sedimentary structures

found.

It is a s s u m e d

that the l a m i n o i d s o r i g i n a t e d in a quiet,

are c o m m o n l y i d e n t i c a l w i t h those of the

s h a l l o w s u b t i d a l to s u p r a t i d a l h y p e r s a l i n e

Zechstein Platy Dolomite

environment

for w h i c h a m i c r o -

b i a l o r i g i n has b e e n i n f e r r e d et al.

(GASIEWICZ

1986). S t r o m a t o l i t e s d i f f e r from

the l a m i n o i d rocks

in that they h a v e c l e a r l y

systems

c o m p a r a b l e to r e c e n t s a b k h a

(GASIEWICZ et al.

1986),

163

Lump

DEPOSITIONAL SEQUENCE

lithofacies

Rocks i n c l u d e d in the lump l i t h o f a c i e s occur c o m m o n l y in the c e n t r a l part of the area studied,

P r i o r to the d e p o s i t i o n of the Main Do-

in a zone e x t e n d i n g from the

lomite,

the area was

slightly inclined

C h l a p o w o t h r o u g h C z a r n y M l y n and S u l i c i c e

wards

to Klanino.

sequent marine transgressions

The rocks are u s u a l l y of grain-

stone texture, 30),

including

lumps

(ILLING 1954:

(PERYT et al.

to-

1985). The subtook place

in several stages.

almost totally m i c r i t i z e d poorly sort-

ed grains

(which have a d i a m e t e r up to a

few m i l l i m e t e r s ) , and v a d o i d s ostracods, (Plates

w i t h rare ooids,

and sparse b i o c l a s t s bivalves

31/I-3;

~hofacies

and

32/I-2;

clasts

The first t r a n s g r e s s i o n s u b m e r g e d the

peloids

s o u t h e r n part of the region as far n o r t h

including

as to a line e x t e n d i n g from S w a r z e w o through

rare d a s y c l a d a c e a n s

Zdrada-Polczyno

37/I). The lump li-

(Plates 31/4;

(Plate 31/3).

35/I),

and K l a n i n o to S u l i c i c e

(Fig. 9A) and then to Kopalino.

in the l o w e r m o s t part of the Zech-

stein Main D o l o m i t e often c o n t a i n s

eyes

the SE

g r e s s i o n h a l t e d here

intra-

facies

and rare b i r d s -

The trans-

long enough

z o n a t i o n to develop.

for a

In the n o r t h e r n -

m o s t part of the flooded area p e l o i d a l -

In recent e n v i r o n m e n t s

i n t r a c l a s f i c p a c k s t o n e s w e r e formed,

lumps usually form in s h a l l o w s u b t i d a l and

exhibiting fenestral

intertidal environments with restricted

nate w i t h thin very f o s s i l i f e r o u s

circulation

(FLUGEL 1982).

A s i m i l a r en-

presumed

visaged

deposits

for the d e p o s i t i o n a l e n v i r o n m e n t of

of m i c r i t i z a t i o n

They alter-

containing a diverse open-marine

v i r o n m e n t w i t h i n c r e a s e d s a l i n i t y is en-

the M a i n D o l o m i t e lump grainstones.

fabrics.

Because

layers fauna

to have b e e n d e p o s i t e d as s t o r m (Zdrada IG8 well).

clastic wackestones

it is d i f f i c u l t to recog-

often

Peloidal-bio-

to p a c k s t o n e s

p a n i e d by s t r o m a t o l i t e s

nize the p r i m a r y n a t u r e of m o s t of the lumps,

stones,

but in some cases f r a g m e n t s of d a s y c l a d a -

subtidal environments

representing

accom-

and o o i d g r a i n -

intertidal

and s h a l l o w

(Zdrada IG3 and Zdra-

ceans can be r e c o g n i z e d as lump c o n s t i t u e n t s

da IG5 wells),

(Plate 32/I). Some lumps p o s s e s s i r r e g u l a r

w i d e w h i c h ran p a r a l l e l to the coast.

s l i g h t l y c r e n u l a t e d shapes,

F u r t h e r to the south,

sent m i c r i t i z e d vadoids;

and may r e p r e -

v a d o i d s of s i m i l a r

formed a b e l t several km

shape c o m m o n l y o c c u r in the grainstones.

peloidal wackestones

In the l i t h o f a c i e s

ki IG2 well)

as a whole,

crusts are q u i t e c o m m o n

cement

(Plate 31/I)

at the b e g i n n i n g of

the Main D o l o m i t e d e p o s i t i o n ,

and

(Mechelin-

and it may be s u p p o s e d that

the t r a n s g r e s s i o n

i n d i c a t e that the p e r i o d s of s e d i m e n t a t i o n

subtidal

accumulated

in that area was so rapid

that tidal d e p o s i t s n e v e r w e r e

formed.

a l t e r n a t e d w i t h p e r i o d s od n o n - d e p o s i t i o n and cementation.

The e x t e n t of the first t r a n s g r e s s i o n was p r o b a b l y c o n t r o l l e d by the i n h e r i t e d

!4uddy l i t h o f a c i e s The m u d d y

topography:

lithofacies comprises mudstones

and o c c a s i o n a l p e l o i d - b i o c l a s t i c w a c k e s t o n e s . Mudstones

are u n l a m i n a t e d and h o m o g e n o u s

or show p a r a l l e l ous material:

la~nination w i t h t e r r i g e n -

q u a r t z grains

r e g i o n and clay m i n e r a l s

in the e a s t e r n part of the

area s t u d i e d w h e r e good,

the w e l l control

is very

the r e c o n s t r u c t e d coast line follows

the 22 m i s o p a c h of the U p p e r A n h y d r i t e deposits

(PERYT 1986

: Fig.

I).

in the Leba

and s i l t - s i z e d

A rise of s e a - l e v e l c a u s e d a m i g r a t i o n

quartz grains in the central p a r t of the

of the coast towards the n o r t h - e a s t and

area studied.

the w e s t as far as Leba, w h e r e m a i n l y

T h e y c o n t a i n a sparse fauna

(bivalves and gastropods)

and are i n f e r r e d

in-

t e r t i d a l d e p o s i t s of the s a b k h a s y s t e m

to have b e e n d e p o s i t e d in a q u i e t s u b a q u e o u s

formed

environment.

open m a r i n e d e p o s i t s -

(Fig. 9 B).

I n i t i a l l y at K o p a l i n o accumulated,

but later

p e r h a p s a f t e r very small sea level falls -

a coastal o o l i t i c b a r r i e r s y s t e m d e v e l o p e d h e r e and s t a r t e d to p r o g r a d e r e l a t i v e l y quickly,

finally r e a c h i n g the area SE of

164

165

\

__,ost t%er l; y s tern

\

~.

~stal

C

q

lagoon " "\

sabkha

""

"

.~

coastal oolitic barrier system

_

9

I

\

\ D .'\..

.

0 ~

land\

/ /

I

J

\ se, \

\ \

Fig. 9. A, B, C, D. Paleogeography during the phases of Main Dolomite deposition.

166

S l a w o s z y n k o ONZI (Fig. 9 C) 9 F u r t h e r to the s o u t h - e a s t r e s t r i c t e d shelf d e p o s i t s m u l a t e d which,

accum-

a f t e r the rapid d e v e l o p m e n t

it is hard to relate the M a i n D o l o m i t e sections of the Leba and K o p a l i n o regions. The d e p o s i t i o n of the s u l p h a t e unit at L e b a

of the p l a t f o r m edge o o l i t i c barrier,

and the r e p l a c i v e s u l p h a t e s

at K o p a l i n o

became

may r e p r e s e n t a h y p e r s a l i n e

gypsum-precip-

l a g o o n a l in character.

itating lagoonal environment which This p l a t f o r m edge b a r r i e r was not re-

suffered

d e s t r u c t i o n d u r i n g e x p o s u r e and m e t e o r i c

c o r d e d in the b o r e h o l e s but its a p p a r e n t

dissolution.

a b s e n c e can be e x p l a i n e d by the small w i d t h

phates s a t u r a t e d and r e p l a c e d the under-

of the p l a t f o r m edge sands.

The d i f f e r e n c e s

The r e d i s t r i b u t i o n of the sul-

lying o o l i t i c carbonates.

South of L e b a V I

in the o c c u r r e n c e of layers c o n t a i n i n g

w e l l in the B i a l o g a r d a IGI and L e b o r k IGI

vadoids

wells

and b e a c h r o c k

fragments

and the

the d o l o m i t e s

are m i s s i n g c o m p l e t e l y

d e g r e e of r e s t r i c t i o n as e v i d e n c e d by the

as only s u l p h a t e s w e r e d e p o s i t e d d u r i n g the

closely s p a c e d boreholes,

M a i n D o l o m i t e time.

s e e m to i n d i c a t e

that the b a r r i e r was m i g r a t i n g

in r e s p o n s e

to small sea level fluctuations. able l o c a t i o n is shown in Fig. ply of

vadoids and b e a c h r o c k

Its prob-

The shift of c a r b o n a t e

d e p o s i t i o n was r e c o r d e d in the L e b a VI w e l l (Fig. 4 ).

9 C. The sup-

fragments

to

It has b e e n s u g g e s t e d e a r l i e r that the

the lagoon was p r o b a b l y r e l a t e d to s t o r m

c o a s t a l o o l i t i c b a r r i e r s y s t e m r e a c h e d the

activity.

region south of Slawoszynko,

and that a

s y s t e m of p l a t f o r m - e d g e o o l i t i c bars had In the area l o c a t e d south of the b a r r i e r edge,

open m a r i n e b i o c l a s t i c and p e l o i d a l

wackestones

a c c u m u l a t e d and a l t h o u g h there

are d i f f e r e n c e s

no e v i d e n c e has b e e n

in that area,

found for s u b a e r i a l

e x p o s u r e d u r i n g M a i n D o l o m i t e deposition.

B e t w e e n these sand shoals

ly p e l o i d a l and i n t r a c l a s t i c p a c k s t o n e s they are s o m e t i m e s

by the o c c a s i o n a l s u b a e r i a l e x p o s u r e s oolitic barriers

of

and the v a d o s e d i a g e n e s i s

local oolitic bars.

T h e s e bars,

m a i n source of v a d o i d i n t e r c a l a t i o n s w h i c h are often a s s o c i a t e d w i t h

lagoonal deposits.

Those g r a i n s t o n e bars w e r e also s u b j e c t e d to p e r v a s i v e v a d o s e d i a g e n e s i s iods of s e a - l e v e l

m a r k sea level rises.

as w e l l as

o o l i t i c bar, w e r e the

s y s t e m it is p o s s i b l e to d i s t i n g u i s h lagoonal d e p o s i t s w h i c h often

and

s t r o m a t o l i t e s w h i c h m o s t likely r e p r e s e n t

of ooids. W i t h i n the c o a s t a l o o l i t i c b a r r i e r

of v a d o s e diagenesis;

ac-

accompanied

by thin c o m p l e x e s of ooid g r a i n s t o n e s

the p l a t f o r m - e d g e Sea level f l u c t u a t i o n s are d e m o n s t r a t e d

a

l a g o o n a l e n v i r o n m e n t e x i s t e d in w h i c h m a i n -

cumulated;

in the d e v e l o p m e n t and

s e q u e n c e of the l i t h o f a c i e s

formed there.

d u r i n g per-

fall.

follow the periods

accordingly, However,

they

it is not

The topmost part of the M a i n D o l o m i t e s e q u e n c e was e r o d e d on m o s t parts of the

p o s s i b l e to c o r r e l a t e those c h a n g e s e v e n

c a r b o n a t e p l a t f o r m p r i o r to the d e p o s i t i o n

in c l o s e l y

of the P l a t y Dolomite,

located b o r e h o l e s

it is a s s u m e d that those

and t h e r e f o r e

surfaces showing

and is p r e s e r v e d

only in the o u t e r part of the c a r b o n a t e

an e x p o s u r e h a v e only a l i m i t e d p o t e n t i a l

platform,

to be u s e d for correlation.

rare

where peloidal packstones

ooid g r a i n s t o n e s

and

top the sequence. The

M a i n D o l o m i t e d e p o s i t s are covered by reIn K o p a l i n o ,

p a r t of the c o a s t a l o o l i t i c

c o m p l e x is r e p l a c e d by sulphates. of that r e p l a c e m e n t is unknown, - w e s t of Kopalino,

The timing

but south-

in the v i c i n i t y of Leba,

crystallized

laminated sulphates

of a d e p o s i t i o n in a s a l i n a

indicative

( P E R Y T e t al. 1985).

This s a l i n a o c c u p i e d a d e p r e s s i o n f o r m e d by d i f f e r e n t i a l rates of d e p o s i t i o n b e t w e e n

the

there are two c a r b o n a t e units p r e d o m i n a n t l y

p e r i p h e r a l and c e n t r a l parts of the M a i n Dolo-

c o n s i s t i n g of i n t e r t i d a l d e p o s i t s s e p a r a t e d

m i t e basin. However, local (e.g., in D a r z l u b i e

by a s u l p h a t e u n i t r e p r e s e n t i n g a s a b ~ l a

IGI) c r y p t a l g a l d e p o s i t s i n t h e

environment

i n d i c a t e an i n t e r t i d a l e n v i r o n m e n t and there-

(Fig. 4). B e c a u s e of the frag-

uppermost part

m e n t a r y p r e s e r v a t i o n of the M a i n D o l o m i t e

fore their p r e s e n c e

i n d i c a t e s that t h e d e p o s i -

s u c c e s s i o n s due to the p r e - T r i a s s i c e r o s i o n

tion of the B a s a l A n h y d r i t e w h i c h took p l a c e

167 J under q u i e t s u b a q u e o u s c o n d i t i o n s ceded by a s e a - l e v e l

was pre-

fall at the end of M a i n

D o l o m i t e d e p o s i t i o n and f o l l o w e d by a sealevel rise at the b e g i n n i n g of the B a s a l Anhydrite deposition.

o D B.

To summarize, indicates

the d e p o s i t i o n a l h i s t o r y

that the M a i n D o l o m i t e e x h i b i t s

a shallowing-upward

lithological succession

on the c a r b o a n t e p l a t f o r m that s e d i m e n t a t i o n was

(Fig.

places by small f l u c t u a t i o n s w h i c h are c h a r a c t e r i s t i c c a r b o n a t e platforms. the r e l a t i v e l y

10), and

interrupted

in

of sea level

of m a n y other

This c o n t r a s t s w i t h

large f l u c t u a t i o n s

of sea-

level w h i c h o c c u r r e d d u r i n g the s e d i m e n ~tation of the p r e - e v a p o r i t e c a r b o n a t e the Z e c h s t e i n Limestone. the p a l t f o r m area,

i.e.

In c o n t r a s t to

show a d e e p e n i n g u p w a r d

lithological

-~1

suc0

cession at the b e g i n n i n g of M a i n D o l o m i t e deposition.

&

o

the b a s i n s e q u e n c e s

Although subsequent depositioo -,q

hal h i s t o r y is d i f f i c u l t to interprete, no s h a l l o w i n g - u p w a r d

o

t e n d e n c y has b e e n

r e c o r d e d and they a p p a r e n t l y show a con-

4-1 o

stant d e e p w a t e r d e p o s i t i o n a l e n v i r o n m e n t

J

t h r o u g h o u t the Main D o l o m i t e s u c c e s s i o n

,.-i

or they w e r e d e p o s i t e d u n d e r a p r o g r e s s i v e -

o

B e c a u s e of

o

this d i f f e r e n t b e h a v i o u r of p l a t f o r m and

o .,-i

ly i n c r e a s i n g d e p t h of water.

a d j o i n i n g basin,

the relief b e t w e e n b o t h

o

o o

was a c c e n t u a t e d d u r i n g s e d i m e n t a t i o n of the M a i n D o l o m i t e until at the end of de-

o

p o s i t i o n the relief was e s t i m a t e d to be 40 m. The b a s i n slope was only very s l i g h t ly i n c l i n e d and did not induce any slumping w h i c h is c o m m o n

o'3

in the areas of m o r e q)

a c c e n t u a t e d slopes.

o .i'i

o .,--i 4.1 .,-i ffl o 0j

c >.

B e c a u s e of the unique p a l e o t e c t o n i c a l .,4

s e t t i n g of the area studied, itional t e c t o n i c

o ,-4 o Q

(important in other p a r t s

of the M a i n D o l o m i t e basin) recognized.

the s y n d e p o s -

can not be

o ,-A GJ

.,.4 rd

The p a t t e r n of t h i c k n e s s of

the M a i n D o l o m i t e d e p o s i t s

is d i f f e r e n t

from the p a t t e r n of the faults which, a c c o r d i n g to s e i s m i c data, NW-SE directions & R Y K A 1982).

(MODLINSKI

s h o w W-E and

o

E

1976, K U B I C K I ~4 o

In the area s t u d i e d the base

of PZ2 and the top of PZ3 can be c o r r e l a t e d

m .,..t

@

as w e l l as the b a s e and the top of the en-

S

tire Z e c h s t e i n s e q u e n c e in m o s t parts of the P u c k Bay area, where

except

the e a s t e r n p a r t

the Z e c h s t e i n s e q u e n c e is t h i n n e r

o

~E

g, .r.t

168

(DEBSKI

1983: Figs.

proof therefore,

2, 4). T h e r e

is no

CLARK

that s e d i m e n t a t i o n has

(1980).

Consequently,

s c r i b e d by PISKE

b e e n c o n t r o l l e d by t e c t o n i c s during the

assuming relatively

Main Dolomite deposition

during

sidered,

(1984)

strong sea-level

falls

the Main D o l o m i t e should be reexamined.

a l t h o u g h the u p l i f t e d C e n t r a l

Pomeranian Peninsula fluenced

in the area con-

the m o d e l de-

& SCHRETZENMAYR

(DEPOWSKI

the p a l e o g e o g r a p h y

1978)

The h i s t o r y of s e d i m e n t a t i o n Leba e l e v a t i o n

indicates

in-

at this time.

FACIES MODEL

in the

Considering

that the e x p o s u r e

b a s i n slope

(DEBSKI 1983: Fig.

of c a r b o n a t e p l a t f o r m s was only moderate.

al.

Accordingly,

it may be a s s u m e d that syn-

ly described,

depositional

tectonics c o m p l i c a t e d

a relat-

ively simple h i s t o r y of s e d i m e n t a t i o n t e r p r e t e d by PISKE

& SCHRETZENMAYR

as i n d i c a t i v e of r e l a t i v e l y fluctuations.

in-

(1984)

large s e a - l e v e l

However, b e c a u s e

they b a s e d

1985)

the r e l a t i v e l y u n i f o r m gentle 2; P E R Y T et

and the facies s e q u e n c e p r e v i o u s c o n s i s t i n g of a r g i l l a c e o u s

wackestones/mudstones with whole w h i c h pass s h o r e w a r d s dal-bioclastic

fossils

into peloidal,

and lump deposits

peloi-

and final-

ly into f r i n g i n g oolite tidal flat c o m p l e x e s the L e b a e i e v a t i o n on w h i c h the M a i n Dolo-

their c o n c e p t on studies of the a t t a c h e d

m i t e was d e p o s i t e d may be c a l l e d a h o m o -

c a r b o n a t e platform,

clinal ramp

relations

the p r o b l e m of age

(after READ

1985).

at the base of the M a i n D o l o m i t e

in b o t h cases needs

to be discussed.

In the e n v i r o n s of Leba,

the d e p o s i t s

of the t i d a l - f l a t c o m p l e x c o n s i s t of abunIn the area of the Leba elevation, depositional

h i s t o r y of the lower part of

the M a i n D o l o m i t e c l e a r l y i n d i c a t e s diachronous

the

the

n a t u r e of the base caused by

two rapid rises in sea-level.

The same

was

(PERYT 1983b) w h e r e

it

i n f e r r e d that the initial PZ2 t r a n s g r e s -

laminites

fenestral stromatolites

mite-sulphate

and ocand d o l o -

laminites c h a r a c t e r i s t i c of

a s a b k h a environment.

phate

(PZI) e v a p o r i t e plat-

form in SW P o l a n d

casional

dal w a c k e s t o n e s

rapid rises have b e e n r e c o r d e d on the s l o p e of the W e r r a

dant dolomite microbial

The a s s o c i a t e d p e l o i -

often c o n t a i n a b u n d a n t sul-

laminae as o b s e r v e d

of the s u b t i d a l

in the u p p e r part

zone in the P e r s i a n Gulf

(SHINN 1983). The d o l o m i t e s by sulphates, w h i c h

are a c c o m p a n i e d

form interbeds

sion led to the d e p o s i t i o n of p e r i t i d a l

r e g u l a r streaks,

carbonates

i n t e r b e d s or laminae in m u d s t o n e s .

and o c c a s i o n a l l y v a d o s e d e p o s i t s

in the slope zone,

and that the thin layer

of p e l o i d a l - b i o c l a s t i c

grainstones,

which

siliciclastics

and ir-

and by thin s i l i c i c l a s t i c

underlie

These

the s a b k h a laminites

and are p r o b a b l y of a e o l i a n origin.

is c o m m o n l y o b s e r v e d on the e v a p o r i t e platform

(CLARK 1980),

represents

m a j o r s e a - l e v e l rise.

a second

T h e r e are some areas

S o m e 40 kms w e s t of Leba Z e c h s t e i n dep o s i t s w e r e r e c o r d e d in the U s t k a IGHI bore-

in SW P o l a n d w h i c h w e r e not flooded d u r i n g

hole.

the s e c o n d m a j o r s e a - l e v e l rise but they

low the B u n t s a n d s t e i n

A b o v e the Z e c h s t e i n L i m e s t o n e and bea series of 2~ m e t e r s

are very local. No great r e g r e s s i o n has

of i n t e r b e d d e d c o n g l o m e r a t i c g y p s u m and

been r e c o r d e d d u r i n g the d e p o s i t i o n of the

mudrock

m i d - M a i n D o l o m i t e in that or other areas

sequence a

(CLARK 1980, M A N N et al.

CLARK & TALLBACKA 1978)

and it seems

occurs. In the upper p a r t of this layer (0.7 m thick)

of d o l o m i t e

1980, S A N N E -

s u l p h a t e l a m i n i t e of s a b k h a type occurs

that the

which may correspond

M a i n D o l o m i t e of the L e b a e l e v a t i o n is a

to the M a i n D o l o m i t e

s a b k h a flat.

c o u n t e r p a r t of the s e q u e n c e s d e p o s i t e d on the a t t a c h e d c a r b o n a t e p l a t f o r m s parts of the basin, by PISKE

in other

i n c l u d i n g those s t u d i e d

& SCHRETZENMAYR

p r o b a b l y it c o m p r i s e s

(1984),

and m o s t

the lower p a r t of the

A tidal flat c o m p l e x r e c o r d e d in the vici n i t i y of L e b a passes b a s i n w a r d s

into

o o l i t i c - p e l l e t sand flat d e p o s i t s w h i c h w e r e r e c o r d e d in the Kopalino,

Debki, W i d o w o a n d

M a i n D o l o m i t e s e q u e n c e c o m m e n c i n g w i t h the

Slawoszynko

b o r e h o l e s . T h e y o c c u r in a zone

d e p o s i t i o n of the "basal c a r b o n a t e s " sensu

a b o u t 20 k m

wide,

and pass

into p e l o i d a l

169

-bioclastic tain

i n t e r b e d s of vadolites,

p e r i o d s of shallowing.

This

f o r m in w a t e r s e v e r a l

to 10 m e t e r s d e e p in the P e r s i a n Gulf

indicating

REAU & P U R S E R

facies seems

to r e p r e s e n t a lagoonal e n v i r o n m e n t , ever,

and w a c k e s t o n e s w h i c h

and lump d e p o s i t s w h i c h con-

1973)

(HAGAN & L O G A N

how-

1974),

s e a w a r d of the fring-

ing o o l i t i c sand flats.

a b a r r i e r c o m p l e x w h i c h w o u l d separ-

(LO-

and in H a m e l i n Pool

3 e c a u s e of d i f f e r e n t

ate the lagoon from the d e e p e r ramp facies

rates of s e d i m e n t a t i o n on p a r t of the ramp

was not r e c o r d e d in the cores and r e m a i n s

a d j o i n i n g the f r i n g i n g o o i d - s h o a l

speculative.

and in the c e n t r a l p a r t of the P e r i - B a l t i c

It is p o s s i b l e

p e l l e t b a r r i e r complex,

that the ooid-

Gulf,

r e c o r d e d in the

X o p a l i n o and Debki boreholes,

prograded

(Figs.

9C,

10) e v e n t u a l l y

the d e p t h in

to e x c e e d 40 m e t e r s

at the end of the Main D o l o m i t e deposition.

s e a w a r d d u r i n g d e p o s i t i o n of the Main Dolomite

SE of the area studied,

the latter area seems

complex

reaching

a line to the w e s t of the Czarny Mlyn IGI, A C K N O W L E D G M E N T S

R a d o s z e w o IGI and K l a n i n o IG2 boreholes. S o u t h - e a s t of this

line and s e a - w a r d of the I w a n t to thank the A l e x a n d e r von H u m b o l d t -

o o i d - p e l l e t b a r r i e r c o m p l e x open m a r i n e (essentially mud supported) which

Stiftung

are d e p o s i t e d

p r i n t i n g costs,

form a l m o s t the entire s e q u e n c e of

the M a i n D o l o m i t e section Slawoszynko boreholes, deposits,

for a f e l l o w s h i p and part the

of the

I n s t i t u t e of G e o l o g y

U n i v e r s i t ~ t F r e i b u r g i. Br., J. Debski, M. Ry-

in the W i d o w o and

bicki,

and r e p r e s e n t ramp

ments

s i m i l a r to the s k e l e t a l p a c k s t o n e s

M. Bejger, and T. P e t t i g r e w

for com-

and d i s c u s s i o n and t e c h n i c a l help.

R E F E R E N C E S CLARK,

D.N.

(1980):

Drenthe, CLARK~

the

D.N.

& TALLBACKA,

Sedimentology, CZAPOWSKI,

The s e d i m e n t o l o g i e

Netherlands. - Contr.

9,

L.

T.M.

J.

Prz.

(1983):

24 Figs.,

S.

293-299,

(1978, ed.):

28 Figs.,

P.W., DEPOWSKI,

eds.~

o k o l i c a c h Leby.

- Kwart.

Geol., 28,

752-~53, W a r s z a w a

cze~ci w y n i e s i e n i a Leby.

litofacjalno-paleogeograficzny permu obszar6w platformo-

Fore-Sudetic

T.M.,

area, w e s t e r n Poland.

PIATKOWSKI,

T.S.

& WAGNER,

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- In: ROEHL, P.O. New York

R.

26, ,

(Springer)

- Prz.

Geol.,

141-146, 4 Figs., W a r s z a w a & -- (1981): P a l e o g e o g r a p h y versus oil and gas p o t e n t i a l of the Z e c h s t e i n M a i n

Dolomite

in the P o l i s h Lowland.

- Proc.

Intern.

Symp.

C e n t r a l Europ.

3 Figs, W a r s z a w a (Wyd. Geol.) ENOS, P. (1974): S u r f a c e s e d i m e n t facies map of the F l o r i d a - B a h a m a s Amer., --

& CHOQUETTE,

(1978): S e d y m e n t a c j a i p a l e o g e o -

g r a f i a c e c h s z t y ~ s k i e g o d o l o m i t u g l 6 w n e g o a jego ropo- i gazonow167

,

-

5 Figs., W a r s z a w a

Atlas

C a r b o n a t e P e t r o l e u m Reservoirs, 253-264,

S., PERYT,

- Contr.

u t w o r 6 w z p o g r a n i c z a cech-

w y c h Polski. - Wyd. Geol., W a r s z a w a DEPOWSKI, S. & PERYT, T.M. (1985): C a r b o n a t e p e t r o l e u m r e s e r v o i r s of the Zechstein,

Stuttgart

Stuttgart

Zarys s t r a t y g r a f i i c e c h s z t y n u we w s c h o d n i e j

Geol., 31,

DEPOWSKI,

131-165,

(1984): S r o d o w i s k a s e d y m e n t a c j i

sztyni i p s t r e g o p i a s k o w c a w DEBSKI,

9,

(1980): The Z e c h s t e i n d e p o s i t s of s o u t h e r n Denmark.

205-231,

G. & PERYT,

of the Z e c h s t e i n 2 C a r b o n a t e F o r m a t i o n of e a s t e r n Sedimentology,

Map Series,

MC-5,

- Am. Assoc.

Petrol.

Geol. Mem., 33,

Tables, T u l s a FLUGEL, E (1982): M i c r o f a c i e s A n a l y s i s of L i m e s t o n e s . Tables,

Berlin - Heidelberg - New York H.

(1964): Fazies,

s c h e n Zechsteins. GASIEWICZ,

A.,

GERDES,

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Soc.

- 633 pp.,

267-295,

78 Figs.,

25 Figs., 2

53 Plates,

58

(Springer)

P o r o s i t ~ t und G a s i n h a l t der K a r b o n a t g e s t e i n e des n o r d d e u t -

- Z. dt. geol.

Ges., 114,

G. & KRUMBEIN,

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n o d u l e facies - b i o g e n i c c a r b o n a t e s the G a v i s h Sabkha,

Plateau.

587-595,

4 p.

(1983): Shelf environment.

FUCHTBAUER,

Permian,

484-531,

Pls.

17-18,

12 Figs.,

Hannover

(1986): The p e r i t i d a l s a b k h a type b i o l a m i n o i d -

in the P l a t y D o l o m i t e

Sinai - A comparative study.--

(Permian), N o r t h P o l a n d and

(submitted)

170 HAGAN,

G.M.

Shark HARRIS,

& LOGAN,

Bay,

P.M.

!,

(1979):

163 pp.,

ILLING,

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1-95,

57 Figs.,

S.

Development

of c a r b o n a t e

- Am. Assoc.

anatomy

Petrol.

and d i a g e n e s i s

banks

Geol.,

and h y p e r s a l i n e

Mem.,

of a B a h a m i a n

basins,

2~2, 61-139,

ooid

shoal.

Tulsa

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Miami

Bahaman

& RYKA,

calcareous

MODLINSKI,

W.

& PURSER,

Z.

Gulf.

(1976):

baltyckiej. T.M.

sands.

- Amer.

25,

geologiczny

Assoc.

Petrol.

Geol.

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PURSER,

B.H.

Inst.

Stromatolity

Vadoids.

Berlin

(Springer) Osady

--

(1983b):

--

(1984):

--

(1985a) : C h e m i c a l

31,

zagadnienia

Geol.,

Pls.

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ed.:

Bull.,

38,

T.M.,

252-254,

2 Figs.,

Sedymentacja

of H o l o e e n e

- 279-328,

zachodniej

Berlin

cze~ci

ooids

in

(Springer)

syneklizy

pery-

cechszty~skim

monokliny

przedsudeckiej.

- Kwart.

Warszawa Grains.

dolomicie

- 437-449,

gl6wnym

7 Figs.,

(Ca 2) o k o l i c

I Table,

Kalisza.

- Prz.

Warszawa

i wczesna

diageneza

chodniej. - P r a c e Inst. Geol.,

109

utwor6w wapienia

80 pp.,

control

of c a r b o n a t e

ooids

of s o u t h e a s t e r n

calcite-aragonite

czesci

Warszawa

ed.: C o a t e d

caliche w cechszty~skim

Gulf:

strukturalne

2 Tables,

PERYT,

Persian

polskiej

Warszawa

and u l t r a s t r u c t u r e

27___O0, 37-48,

w wapieniu

I-6,

krystalicznego

Geologiczny,

Distribution

Niekt~re

podloza

- Instytut

(1973):

609-628,

(1983a):

Geol.,

Atlas

B.H.

- Biul

(1981):

Geol.,

(1982):

wschodnioeuropejskiej.

J.P.

the P e r s i a n

--

Facies

(1954):

platformy

PERYT,

(1974):

Australia.

Tulsa

KUBICKI,

LOREAU,

B.W.

Western

Pls.

1-15,

phases:

cechszty~skiego

31 Figs.,

implication

w Polsce

3 Tables,

za-

Warszawa

from U p p e r P e n n s y l v a n i a n

Kansas

- discussion.

dolomites

of w e s t e r n

- J. Sed.

Petrol.,

55 I

--

(1985b): voirs.

--

PERYT,

T.M.,

northern

B.J.

Bahamas. J.

(1980):

B.H.

69,

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(1985):

1-21,

-

W.

SCHOLLE,

44, SHINN,

~, WILSON,

D.B.

5 Figs.,

carbonates 359-360,

ewaporatow

Warszawa

of the s o u t h e a s t e r n

Marseille

Wiss., dans

12,

83-100,

les s~ries

und

7 Figs.,

ihre Berlin

carbonat~es

du

383 pp.

n~ritiques

recents,

vol.

I, 366 pp.,

J.

H.

Ges.,

(1977): 47,

& KINSMAN,

8 Figs.,

(1983):

B.H.

Ges.,

platform

& PLEIN,

geol.

Petrol.,

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: The Persian

114,

facies

encrustations

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343-376,

Hauptdolomits

461-483, models.

Pls.

12-16,

- Amer.

on the T r u c i a l Berlin

im Z e c h s t e i n 4 Figs.,

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Assoc.

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ZIMDARS,

904-916, E.A.

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sedymentacji

im S t a s s f u r t k a r b o n a t

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E.

(1978):

129,

33-69,

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600-609,

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52 Figs., SMITH,

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& BOLZ,

P.A.

Persian

(1973):

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Petrographie

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J. Sed.

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Technip)

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204-211,

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1986,

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SANNEMANN,

SCHLAGER,

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(1985):

Geol,

et d i a g ~ n ~ s e p r ~ c o c e

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Poland:

Reading

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(Ed.

Coast, QUESTER,

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463-474,

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& SCHRETZENMAYR,

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8,

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Modifikation PURSER,

Geol.,

CZAPOWSKI,

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PIERSON,

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Permian

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11 Figs.,

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Der b a s a l e Pls.

7 Figs.,

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Weser

Hannover evaporites

in d e e p w a t e r

Tulsa

Aragonitic

for the P e r m i a n

and h i g h - M g of Texas

calcite

caliche

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from

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Petrol.

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- Amer.

Assoc.

Petrol.

Geol. M~m., 3_/3, 171-210,

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7-34,

2 Figs.,

J.L.

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Zechstein

basin.

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Sedimentology,

Stuttgart Carbonate

Facies

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History.

- 471 pp., B e r l i n

(Springer)

172

Plate

24

Z e c h s t e i n M a i n Dolomite,

Leba E l e v a t i o n ,

Northern Poland

Zechstein-Hauptdolomit, Leba-Schwelle,Nordpolen Note:

unless s p e c i f i e d the rocks p r e s e n t e d on Plates

are dolomites.

Fig.

I.

P e l o i d a l p a c k s t o n e w i t h pores (now filled w i t h g y p s u m - w h i t e areas) and small quartz grains (small w h i t e dots). N o t i c e the v a r y i n g size of the peloids. The rock seems to be i n t e n s e l y b i o t u r b a t e d (arrows). L e b a IV well, depth 529.2 m. x 10

Fig.

2

B i o c l a s t i c w a c k e s t o n e , w i t h m o u l d s (now filled w i t h gypsum) rare gastropods. L e b a V well, d e p t h 575.9 m. x 8.3

Fig.

3.

Limestone: d e d o l o m i t i z e d p e l o i d a l - b i o c l a s t i c K l a n i n o IG2 well, d e p t h 676.1 m. x 10

Fig.

4

D o l o m i t i c limestone: d e d o l o m i t i z e d l u m p - p e l o i d a l - o o i d a l grainstone. The d e d o l o m i t i z a t i o n a f f e c t e d m a i n l y the cement, and in p l a c e s also the ooids~ The process is a c c o m p a n i e d by c a l c i t i z a t i o n of sulphates. R a d o s z e w o IGI well, d e p t h 671.8 m. x 10

Fig.

5

Detail of the t h i n - s e c t i o n shown in Fig. 4. N o t i c e the vague texture of an ooid (top center) and the c a l c i t e in the ooid c o r t e x (large grey crystals),

Fig.

6

of b i v a l v e s

and

p a c k s t o n e w i t h bivalves.

x 67

Ooidal g r a i n s t o n e r e p l a c i n g gypsum. In places only streaks of the o r i g i n a l rock texture are p r e s e r v e d in a thick bed (see Text-Fig. 5) of r e p a c e d sulphates. K o p a l i n o IGI well, d e p t h 541.3. x 9.8

Length of the thin bar:

2mm;

length of the thick bar 0.2 mm

TAFEL 24

174

25

Plate

Zechstein

Main

Dolomite,

Zechstein-Hauptdolomit,

Leba E l e v a t i o n t N o r t h e r n

Poland

Leba-Schwelle, Nordpolen

Fig.

I.

P e l o i d a l p a c k s t o n e w i t h b i v a l v e s , gastropods, ostracods, u n i s e r i a l and e n c r u s t ing f o r a m i n i f e r s , and a b u n d a n t pores (mainly m o u l d s of bioclasts) w h i c h are now filled w i t h anhydrite. Z d r a d a IG8 well, d e p t h 752.1 m. x 10

Fig.

2.

Peloidal chelinki

Fig.

3.

Detail

Fig.

4.

Peloidal chelinki

Fig.

5.

Length

packstone IG2 well,

of d a s y c l a d a c e a n s m. x 10

and o c c a s i o n a l

bivalves.

Me-

with moulds d e p t h 957.6

of d a s y c l a d a c e a n s m. x 10

and o c c a s i o n a l

bivalves.

Me-

Peloidal packstone with moulds well, d e p t h 819.1 m. x 10

of d a s y c l a d a c e a n s

and bivalves.

of Fig.

I. x 125

packstone IG2 well,

of the thin bar:

with moulds d e p t h 958.2

2 mm;

length

of the

thick bar:

0.2 m m

Darzlubie

IGI

TAFEL 25

176

26

Plate

Z e c h s t e i n Main Dolomite,

Leba Elevation,

Northern Poland

Zechstein-Hauptdolomit, Leba-Schwelle, Nordpolen Fig.

I9

O o i d a l - p e l o i d a l - b i o c l a s t i c g r a i n s t o n e w i t h bivalves, b r a c h i o p o d s , and gastropods. N o t i c e p e l o i d a l i n f i l l i n g u n d e r n e a t h b i v a l v e shells. The i n c r u s t a t i o n s are s o m e t i m e s a c c o m p a n i e d by e n c r u s t i n g f o r a m i n i f e r s . Zdrada IG5 well, d e p t h 754.8 m. x 10

Fig.

2.

C o m p o s i t e o o i d of s o m e w h a t c e r e b r o i d shape. The ooids (composite and simple) w i t h these shapes w e r e found in the lower p o r t i o n of the Main D o l o m i t e in the Z d r a d a - S w a r z e w o area only, they are often a c c o m p a n i e d by m i c r o b i a l deposits. The o o i d c o r t e x c o n s i s t of a l t e r n a t i n g m i c r i t e and s p a r i t e laminae and is s i m i l a r to the c o a t i n g of some b i o c l a s t s in b e a c h d e p o s i t s w h e r e the e v a p o r a tion of s p l a s h i n g w a t e r led to p r e c i p i t a t i o n of m i c r i t e and sparite laminae. Zdrada IG5 well, d e p t h 754.7 m. x 67

Fig.

3.

Detail of Fig. 4. D a r k d i s c o n t i n u o u s crusts (arrows) p r e c e d i n g a t i o n have the same fabric as ooids shown in Fig. 2. x 67

Fig.

4.

A f r a g m e n t of the t h i n - s e c t i o n shown in Fig. I, o u t s i d e the field p r e s e n t e d here (o on Figs. I and 4 i n d i c a t e the same shell), s e v e r a l stages of rim cementation. M o s t w h i t e areas are a n h y d r i t e cement, x 26.7

L e n g t h of the thin bar:

2 ram; length of the thick bar:

0.2 m m

the rim c e m e n t -

TAFEL 26

178

Plate

27


Leba E l e v a t i o n ,

Northern Poland


Figs.

I.

O o i d a l - p e l o i d a l - b i o c l a s t i c g r a i n s t o n e w i t h bivalves, b r a c h i o p o d s , and gastropods, and c a v i t y - f i l l i n g m i c r o b i a l mats i n c l u d i n g small peloids and bioclasts. Arrows s h o w s y n s e d i m e n t a r y c e m e n t crusts w h i c h are s i m i l a r to the p r i m a r y a r a g o n i t i c cements c o m m o n l y found in the P e r m i a n and T r i a s s i c rocks. Zdrada IG5 well, d e p t h 754.6 m. x 10

2, 3. Details from Fig. I s h o w i n g m i c r o b i a l mats and rim cement on ooids and bioclasts. Fig. 2: x 26.7; Fig. 3: x 67


2 ram; length of the thick b a r 0.2 m m

TAFEL 27

180

28

Plate

Zechstein Main Dolomite,

Leba Elevation,

Northern Poland


I9

Shell fragment coated with alternating micrite and sparite cement crust and then broken; the breaking most probably occurred during burial. Zdrada IG4 well, depth 789.2 m. x 26.7

Fig.

2.

Peloidal-bioclastic grainstone with bivalves and brachiopods; the latter are often coated with alternating micritic and sparitic cement. The bivalve shells in the upper part of the picture have been afterwards broken by compaction. Zdrada IG5 well, depth 754.8 m. x 10

Fig.

3.

Peloidal-bioclastic packstone with brachiopods, bivalves, ostracods, gastropods and encrusting foraminifers. White area on the photo is anhydrite cement. Starzyno IG2 well, depth 718.0 m. x 10

Fig.

4.

Peloidal-bioclastic packstone with abundant gastropods (notice several cement generations) and bivalves, encrusting foraminifera and ostracods. Swarzewo IG8 well, depth 740.9 m. x 10

Fig.

5.

Detail of Fig.


4. White area is anhydrite cement,

2 mm;

length of the thick bar 0.2 m m

x 26.7

TAFEL 28

182

29

Plate


Leba Elevation,

Northern Poland


I.

Peloidal-bioclastic packstone with ostracods, bivalves (arrows). Opalino IG1 well, depth 748.0 m. x 10

Fig.

2.

Peloidal-ooidal-bioclastic grainstone; pores are filled with anhydrite areas). Swarzewo IG8 well, depth 741.1 m. x 10

Fig.

3.

Peloidal-bioclastic grainstone with M~zz~a fragments (arrow), bivalves, gastropods, ostracods, encrusting foraminifers. Lumps are fairly common in this facies locally. Zdrada IG4 well, depth 790.8 m. x 14.4

Length of the thin bar: 2 mm;

length of the thick bar: 0.2 m m

and dasycladaceans (white

TAFEL 29

184

Plate

30


L e b a Elevation,

Northern Poland


I.

P l a n a r b e d d e d ooidal g r a i n s t o n e w i t h i n t r a c l a s t s (i) of o o i d a l grainstone; i n t r a c l a s t s are o c c a s i o n a l l y coated. A r r o w i n d i c a t e s grains shown in P l a t e 37/4. M i l o s z e w o ONZl well, d e p t h 1223.4 m. x 10

Figs.

2, 3. O o i d a l g r a i n s t o n e rich in c o m p a c t i o n p h e n o m e n a w h i c h w e r e p r e c e d e d by cement A formation. K o p a l i n o IGI well, d e p t h 549.3 m. Fig. 2: x 10; Fig. 3: x 67

Figs.

4, 5. O o i d a l g r a i n s t o n e w i t h a b u n d a n t lumps of b e a c h r o c k . In ooidal g r a i n s t o n e s c o m p a c t i o n can be e s p e c i a l l y w e l l observed. Czarny M l y n IGI well, d e p t h 616.0 m. Fig. 4: x 26.7; Fig. 5: x 67


2 ram; length of the t h i c k bar 0.2 m m

TAFEL 30

186

31

Plate



Leba Elevation,

Northern Poland


Fig.

I9

L u m p - p e l o i d a l p a c k s t o n e - g r a i n s t o n e . N o t i c e c o m p a c t i o n of grains in the upper right corner and c e m e n t crusts (arrows). K l a n i n o IG2 well, depth 670.1 m. x 10

Fig.

2.

L u m p - p e l o i d a l packstone.

Fig.

3.

L a m i n o i d - p e l o i d a l p a c k s t o n e w i t h b i r d s e y e s t r u c t u r e s and grains (vadoids) exh i b i t i n g a c o a t i n g c o m p o s e d of a l t e r n a t i n g m i c r i t e and s p a r i t e laminae (arrows). K l a n i n o IG2 well, d e p t h 706.2 m. x 10

Fig.

4.

I n t r a c l a s t s of p e l o i d a l packstone. Rim c e m e n t in the small d i s s o l u t i o n pores (arrows), now m o s t l y filled w i t h gypsum. K o p a l i n o IGI well, depth 561.2 mo x 26.7


2 mm;

C z a r n y Mlyn IG1 well,

length of the thick bar:

d e p t h 630.4 m. x 10

0.2 m m

TAFEL 31

188

Plate

32



Leba Elevation,

Northern Poland


Fig.

I.

Lump-peloidal grainstone. Some lumps are micritized dasycladaceans Sulicice IG2 well, depth 673.5 m. x 10

Fig.

2.

Ooidal-lump packstone with common distorted grains (partly vadoids?) overlying (cracked?) peloidal wackestone. Chlapowo IG4 well, depth 658.4 m. x lO

Fig.

3.

Ooidal-peloidal-bioclastic grainstone overlain by stromatolite containing laminae of encrusting foraminifers. Zdrada IG5 well, depth 754.6 m. x 10

Fig.

4.

Foraminiferal encrustations related to stromatolitic boundstones (which underlie and overlie the field of the photo). Notice the rare serpulids (arrows). Swarzewo IG8 well, depth 740.7 m. x 26.7


2 mm;

length of the thick bar: 0.2 mm

(arrows).

TAFEL 32

190

33

Plate


Leba Elevation,

Northern Poland


I9

Laminoidal, p e l o i d a l p a c k s t o n e w i t h c o m m o n moulds of b i o c l a s t s w i t h gypsum). L e b a V well, d e p t h 576.4 m. x 9.5

Fig.

2.

Laminoidal, p e l o i d a l p a c k s t o n e - w a c k e s t o n e w i t h rare Shells 2 well, d e p t h 599.8 m. x 10

Fig.

3.

L a m i n o i d a l , p e l o i d a l p a c k s t o n e w i t h c e m e n t crusts (arrows) and vadoids u p p e r p a r t of the photo. M i l o s z e w o ONZl well, d e p t h 1220.2 m. x 10


2 mm;


0.2 nun

(now filled

(arrows).

Debki

in the

TAFEL 33

192

Plate

34



Leba Elevation,

Northern Poland


Fig.

I.

M i c r o b i a l laminite from the top of the Main D o l o m i t e sequence. well, depth 817.3 m. x 10

Fig.

2.

L a m i n o i d - p e l o i d a l packstone.

Fig.

3.

S t r o m a t o l i t i c b o u n d s t o n e from the b o t t o m of the M a i n Dolomite. In this thins e c t i o n the l a m i n a t i o n is only p o o r l y visible. S w a r z e w o IG8 well, d e p t h 7 4 0 . 5 m . x 10

Fig.

4.

M a g n i f i c a t i o n of a l a m i n o i d - p e l o i d a l packstone. In the m i c r i t i c m a t r i x a b u n d a n t m u m i e s of m a i n l y v e r t i c a l l y o r i e n t e d sheaths of f i l a m e n t o u s m i c r o o r g a n i s m s . S u l i c i c e IG2 well, d e p t h 677.4 m. x 26.7

Fig.

5.

S t r o m a t o l i t i c b o u n d s t o n e and a s s o c i a t e d p e l o i d a l packstone. N o t i c e f r e q u e n t i n c l u s i o n s of p e ! o i d a l m a t e r i a l into the s t r o m a t o l i t i c framework. C z a r n y M l y n IGI well, d e p t h 610.9 m. x 9.7


2 mm;

Debki IGI well,


D a r z l u b i e IGI

d e p t h 570.4 m. x 9.7

0.2 mm

TAFEL 34

194

35

Plate


L e b a Elevation,

Northern Poland


I9

I n t r a c l a s t i c p a c k s t o n e w h i c h often e x h i b i t s l a m i n o i d texture. Some i n t r a c l a s t s c o n t a i n m i c r o b i a l nodules (arrows) and are c h a r a c t e r i z e d by a g r e a t e r p r o p o r t i o n of quartz grains w h e n c o m p a r e d to the p a c k s t o n e matrix. S u l i c i c e IG2 well, d e p t h 693.1. x 10

Fig.

2.

C a l c a r e o u s d o l o m i t e - d e d o l o m i t i z e d l u m p - p e l o i d a l g r a i n s t o n e w i t h bivalves, u n i s e r i a l f o r a m i n i f e r s and a b u n d a n t d a s y c l a d a c e a n s (arrows). R a d o s z e w o IGI well, d e p t h 665.5 m. x 10

Fig.

3.

A f r a g m e n t of a p e l o i d a l - b i o c l a s t i c packstone. The s e d i m e n t is now a d o l o m i t i c l i m e s t o n e w h i c h u n d e r w e n t d e d o l o m i t i z a t i o n . N o t i c e that the d e d o l o m i t i z a t i o n almost c o m p l e t e l y d e s t r o y e d the o r i g i n a l texture. R a d o s z e w o IGI well, depth 673.5 m. x 67

Fig.

4.

L i m e s t o n e - d e d o l o m i t i z e d ooidal g r a i n s t o n e w i t h a b u n d a n t oomoulds. O c c a s i o n ally the c e m e n t e s c a p e d the d e d o l o m i t i z a t i o n process. W i d o w o ONZl well, d e p t h 613.7 m. x 9.7

Fig.

5.

D e t a i l of Fig. 4, s h o w i n g the d e d o l o m i t i z e d ooid cortex (compare the texture w i t h that of the d o l o m i t e ooid in P l a t e 37/4). N o t i c e also that the a r r a n g e m e n t of the c a l c i t e c r y s t a l s follows the p r i m a r y l a y e r i n g of the cortex, and the o c c a s i o n a l d o l o m i t e (= redolomite) crystals (arrow). x 171


2 mm;

length of the thick bar 0.2 m m

TAFEL 35

196

36

Plate


Leba Elevation,

Northern Poland

Z e c h s t e i n - H a u p t d o l o m i t , Leba-Schwelle, Nordpolen Fig.

I.

Ooidal p a c k s t o n e - g r a i n s t o n e w i t h c o n t o r t e d ooids (or vadoids). N o t i c e the sparry c e m e n t b e l o w the grains. M i l o s z e w o ONZl well, d e p t h 1230.5 m. x 10

Fig.

2.

Ooidal g r a i n s t o n e w i t h i n t e r l a y e r i n g f l a t t e n e d grains dowo 0NZl well, d e p t h 616.O m. x 26.7

Fig.

39

P e l o i d a ! - o o i d a l g r a i n s t o n e w i t h f l a t t e n e d grains ONZl well, d e p t h 1219.3 m. x 10

Fig.

4.

O o i d a l g r a i n s t o n e w i t h c o m m o n c o m p a c t i o n features (flattened grains, p a r a l l e l contacts, i n t e r p e n e t r a t i o n of grains). Debki 3 well, depth 581.4 m. x 9.8


2 mm;


0.2 mm

and m o u l d i c pores. Wi-

(probably ooids). M i l o s z e w o

TAFEL 36

198

37

Plate

Zechstein

Main Dolomite,

Leba Elevation,

Northern

Poland


I.

Vadoid p a c k s t o n e w i t h a b u n d a n t

lumps.

Czarny Mlyn IGI well,

depth 617.O m~ x 10

Fig.

2.

Dolomitic limestone - d e d o l o m i t i z e d p e l o i d a l - o o i d a l grainstone. Oomoulds are filled w i t h g y p s u m cement. The ooid cortices e x h i b i t the texture shown in Plate 35/5. S u l i c i c e IG2 well, depth 661.5 m. x 26.7

Fig.

3.

V a d o i d from the upper left corner of Fig. I. N o t i c e the a l t e r n a t i n g sets of m i c r i t i c and sparitic laminae (the latter often u n d e r w e n t d i s s o l u t i o n and subsequent filling by carbonate and s u l p h a t e cements) and the changes of shape during growth, x 67

Fig.

4.

Detail cement of the 1223.4

Fig.

5.

Ooidal grainstone w i t h peloids and lumps. Peloids are strongly r e c r y s t a l l i z e d ooids. Note the s p h e r i c a l shape and traces of the o r i g i n a l c o n c e n t r i c texture in some grains and the c o m p a c t i o n a l grain contacts (arrow). S l a w o s z y n k o ONZl well, d e p t h 612.4 m. x 26.7

of Plate 30/I. Ooid and i n t r a c l a s t grainstone; notice carbonate rim A (dolomite) and sulphate i n t e r g r a n u l a r cement B (FLUGEL 1982); most w h i t e i n t e r s t i t i a l areas are anhydrite. M i l o s z e w o ONZl well, depth m. x 67


2 mm;

length of the thick bar 0.2 mm

TAFEL 37