Zechstein Anhydrites NW of the Holy Cross Mts. (Upper Permian, central Poland): facies and palaeogeography

Geological Quarterly, Vol. 39, No.4, 1995. p. 489-512

Alicja KASPRZYK

Zechstein Anhydrites NW of the Holy Cross Mts. (Upper Permian, central Poland): facies and palaeogeography

The facies variety of the sulphate deposits in the Zechstein of the Holy Cross Mts. reflects distinct sedimentary conditions in the peripheral part of the evnporitic basin. where the cyclic sedimentation of PZl, PZ2, PZ3, and PZ4 was largely affected by input of terrigenous material. In this area two sectors, southern and northern, may be distinguished on the basis of facies zonation. During the evaporite sedimentation, a major area north-west of the Holy Cross Mts. was exposed and affected by intense denudation at low sea level stanps. In the marginal zone, evaporites are lacking and their facies equivalents are siliciclastic deposits. Palaeogeographic and facies patterns were controlled mainly by climatic and tectonic factors.

INTRODUCTION

Throughout geological history giant evaporitic accumulations have been formed under particular climatic and tectonic conditions that occurred in the past but do not exist today (P. Sonnenfeld, 1984). Although no modern analog exists as far as size is concerned, facies comparison has important implications for the interpretation of the sedimentary regime during evaporite deposition

(J.

K. Warren, C. G. S. C. Kendall, 1985; B.

C.

Schreiber, 1988).

Consequently, the facies and sedimentary variety of evaporites are attributed to a wide range of depositional settings, as indicated by the study of modern evaporitic environments, all of which have the common attribute of aridity (e.g. A. V. Arakel, 1980; F. Orti Cabo et aI., 1984; B. W. Logan, 1987; B. H. Purser et al., 1987; C. G. S. C. Kendall, 1. K. Warren, 1988).

The facies succession and lateral distribution of the Zechstein (Upper Permian) deposits north-west of the Holy Cross Mts. (Fig.

1)

are an expression of different basin configuration in the peripheral part of the Polish Basin

(R.

Wagner, 1994). In this area, shallow-water evaporites formed on the shelf whilst in the basin margin sabkha deposition took place

(op.

cit.).

Along with sea-water ingressions, successive deposition of pelites, carbonates and

490 Alicja Kasprzyk

• borehole (a)

Fig. 1. Location of studied boreholes in the area north-west of the Holy Cross Mts.

LokaJizacja zbadanych otwor6w wiertniczych w p6tnocno-zachodnim obrzezeniu G6r .swietokrzyskich 1 - kreda, 2 -jura, 3 - trias, 4 - perm, 5 - paJeozoik G6r Swietokrzyskich, 6 - zasi~g an hydryt6w cechsztynu, 7 - uskok, 8 - otw6r wiertniczy

evaporites resulted in evaporitic sedimentary cycles, which were largely incomplete in the

marginal zone (Z. Kowalczewski, M. Rup, 1989; Z. Kowalczewski, S. Zbroja, in press). As

Zechstein AnI1YOIlres NW of the Holy Cross Mts .... 491

a basinal

"r,""",,,t ... ,,,t'I"r,~"''''.h,'''

correlation of

seC!1mentary

between the

UU.,'-F,LH .... L

and

of the Zechstein basin is difficult and sometimes controversial in a more detailed

~f"\7'''·'',!ll''h (iISCUS:SIO,n

in:

Z. M. R

In this paper the facies and secllmentary used to reconstruct paJlae,oel1vlroTlmcentaJ the

1"\ ... 'nl"1' ... r.,

areas of the Polish Zechstein Basin.

GEOLOGICAL SETTING

salts. and

LV'J"b''''U'-''-'''''

division of the Zechstein formation distinct sulphate

1).

Cross Mts. are from 3 to 760.6 m thick

The succession of facies mr'OuQ"nc)ut

The tectonic framework of the area is characterized

and ESE-WNW fault system linked to late Variscan and

Kowalczewski et

Lithostratigraphic correlation of the Zechstein in the HoJy Cross Mts. Bnd their foreland (after R. Wagner, 1994) Tab 1 e 1

~

HOLY CROSS

Zechstein Anllydr1tesNW of the Holy Cross Mts .... 493

FACIES AND

A

Mts.

PZl ANHYDRITES

LOWER ANHY DRIn::: A It.!

In the southern is 6.0-9.6 m thick

of nodular-mosaic and mosaic "' ....

^{'I-'u .... v}

facies

interbedded with red mudstones and dOllos·tones, which cornmon!

lmlpregn:aucm and nodules I, Nodules are millimetre-centimetre sized and occur isolated or into nodular layers, the relict lamination of the host rock. are connected with each other a dense net of fibrous gypsum veins. Other

sedllmentary structures lamination and biolami-

b'~'~""h'

load structures, and brecciated The transition to

l1nrl""I'IHln

of the Zechstein Limestone and to siliciclastics of the Series Tlr is

In the Nieswiri PIG 1

^{u V} ... H V " .

2260.5-2286.1 m 2264.0-2267.0

massi ve and mosaic

~ n rn/{'rl'1'f'~

banded with

which has palae()enIVlI·onme.nta

50% on of the content

"'-L,",""'~l.Ll"-,", sel~:;ml[eS;

at the top,

UPPER ANHYDRITE A I ^g

";(

"<{

'{~fimif of AJ (231

~

~

II-I--

)< 'A

1961S~

- - ..

'226 - - - -

22B6~A1d

I~ ()~~ clayey-anhydrite b"eccia (1)

~ bio(aminite C2\

10

0 0 0

I

nodular anhydrite (3)

~ nodular-mosaic anhydrite (4)

~ nodular-mosaic beddi?d

~ anhydrite (51

~ mosaic anhydrite <sl

~ banded anhydrite (7) 1 \...v"-'-'~ 1 dourly anhydrite (aJ

CJ

^{massive anhydrite (9')}

~ massive coarse-crystalline

~ anhydrite (10)

~ laminated anhydrite (11)

!j.

~~~

j

skeletal anhyclrite (12)

~ secondary gypsum (13)

~ ^limestone (14)

~ dolostone (15)

~ dolostone with sulphate nodules E3E3 and impregnation (16)

tlaystone (17)

I=~

::--.:1

^{mudstone (18)}

~ claystone} .... ith sulphate nodules (19)

~ mudstone and impregnation (.20)

I:.· .. ·::·:

:1 sandstone (21)

307.1

310~A3 33~1-'-

('1'(

~

⁾⁷

~ ^ry

^SKARZYSKO KAMIENNA

~ ~

^A1g

nl 34t~~A3 ~ T

^)-'CUm'-l

ofAld~\' /

'-'" ^{~A3 ~}

459.~ 359.91 ^{i ' Y}

^~

^t'-~"

(imif olAlg (2S)

362.2

4TII -

^A1g

^{i /}

376, - - - - 0(1<7

~

I,l5.ZS

Mel A1g

'I""-i:

382.0 0 0 362.7 /

4135

----1 Y ~~o~,

~

^SOt "",1jliiI\Ii!Ald

Y

<;4K4 .

8~~A~11

;t

~

~: ~

I'>

-r::

"0 ~

~ _:0;"

Zechstein Anhydrites NW of the Holy Cross MIS ....

495

UnitA is composed of mixed siliciclastic-carbonate-sulphate facies which is transitional between Tlr siliciclastics and overlying sulphate deposits (Fig. 4). Locally in the southern region (Tuml1n Podgrodzie 101, Jaworzna 10 1, Goleniawy 10 1, Lqczna Zaszosie 10 1) there is an alternation of layers, from some centimetres to decimetres thick, of carbonate and sulphate facies. Among them biolaminites as well as nodular and banded sulphate rocks (gypsum and anhydrite) contaminated with clay and carbonate material are dominant, and a11 display irregular clayey-organic lamination. In other sections (Ruda Strawczynska 1, Stachura 10 1, Crninsk 3, Jaworze IG 1) unit

A is composed of red mudstones, locally sandy,

which commonly reveal sulphate impregnation and nodules (often calcified), and minor interbeds of carbonate rocks (limestones, dolostones, marls) (Fig. 2).

Unit B is distinctive in the sequence of the Upper Anhydrite by a presence of clayey- anhydrite breccias and conglomerates 0.45-8.70 m thick. Clasts are slightly abraded or angular fragments, millimetre-centimetre sized, of massive and laminated anhydrites and secondary gypsum, limestones, dolostones, claystones, and mudstones, embedded in a pelitic or clayey-carbonate-sulphate matrix (PI. I, Fig. 11). Aligned, deformed and partly liquefied clasts are common. Locally, packets of sulphate-pelitic-carbonate laminae occur as interbeds within the thicker layers of breccias (J aworze 10 1, Lqczna Zaszosie IG 1). In the Ruda Strawczynska 1 and Tumlin Podgrodzie IO 1 sections the local equivalents of breccias are sandy mudstones with sulphate nodules and impregnation, commonly showing distorted and deformation structures.

Breccias occur throughout the Alg section in different positions: in the middle or lower parts, just at the boundary with the Terrigenous Series TIr (southern region), or in the upper part (Nieswin PIG 1) (Fig. 2). It seems to be a rule that toward the north, with increasing burial, breccias displace upwards through the A 1 g section, and disappear in the central parts of the Zechstein basin (R. \Vagner, 1994).

All features described allow the interpretation of unit B as an equivalent of the PZl Anhydrite Breccia (BrAl), distinguished by R. Wagner (1988) in the lithostratigraphic division of the peripheral parts of the Zechstein basin (Table 1).

In the middle section of the Upper Anhydrite - usually a thick (from 4.1 to 26.2 m) sulphate complex - unit C occurs (Fig. 4). It is composed of massive and mosaic gypsum and anhydrites with common pseudomorphs (up to 5 cm high) after grass-like and cavoli selenites (pt. I, Fig. 12). Locally the transition to laminated, mosaic or bedded nodular-mo- saic varieties, several decimetres thick, is observed. Massive and mosaic anhydrites are dominant lithologies of the Upper Anhydrite in the Nieswin PIG 1 section (Fig. 3). They are lacking in the extreme peripheral areas (Ruda Strawczynska 1 - Fig. 4).

Fig. 2. Lithofacies of the Zechstein Anhydrites in studied boreholes

Wyksztalcenie litofacjalne poziom6w anhydryLowych cechsztynu w badanych otworach wiertniczych I - brekcje anhydrytowo-ilaste, 2 - bio!aminoidy, 3 - anhydryty gruztowe, 4 - anhydryty gruztowo-mozai- kowe, 5 - anhydryty gruztowo-mozaikowe warstwowane, 6 - anhydryty mozaikowe, 7 - anhydryty warstwo- wane, 8 - anhydryty chmurzyste. 9 - anhydryty masywne, 10 - anhydryty masywne grubokrystaliczne, II - anhydryty laminowane, 12 - anhydryty szkieletowe, J 3 - gipsy wt6me, 14 - wapienie. 15 - dolomity. 16- dolomity z gruzlami, 17 - itowce, 18 - mulowce. 19 - ilowce z gruztnmi i impregnacjami siarczanowymi, 20 - mutowce z gruztami i impregnacjami siarczanowymi, 2l - piaskowce, 22 - za<;i<:g anhydryt6w A2. 23 - zasieg nnhydrytu glownego A3. 24 - zasiyg anhydrytu dolnego AJ d. 25 - zasi<;g anhydrytu g6mego Al g

496

S

Alicja Kasprzyk

l\S\Sl

secondary gypsum (1)

t;,,/,,/,/j:1

skeletal anhydrite (2)

II

I

I

^I

II

flaser, mosaic and massive anhydrite (3)

~ P'?~~;;;;;J~~

Cloudy onhydrite (4) laminated anhydrite (5) i banded anhydrite (6)

'-::-ICVl--::--c---'O""----C'J-'1 nodular and nodular- mosaic anhydrite (7)

P.QQ4<3\

'clayey-anhydrite breccia (Sl

~ biolominite (9)

claystone, mudstone with sulphates (10)

~ dolomite with sulphotes (11)

I :::t ^I

^{core locking} (1~

Tumlin Podgrodzle IG 1

A3~

Alg

I

Ca3

T3 T2r

j S

~ ~

I I I I

\.J-J

'-.J..J

~

Cal

N Hleawln PIG 1

Ca3 T3

~A2r

T2r

I I I I I

~~M l~

~ _.06 I

~oo40

I I I I I

A1g

¥

20m

I~ Y-

Ald

Cal

Zechstein l"\.UIIYUl,Uu;:, NW of the Holy Cross Mts ....

In the southern the sequence is terminated

C01np:nSf~S

different SUJpnate lithofacies contaminated with most common varieties are nodular and banded gypsum

with marls and that abound in nodules and ImlJre;gnaltlOn.

is transitional to the Series of PZ2

BASAL ANHYDRITE A2

In the northern

N IP~Ulll n

PIG 1), the facies association of the Basal

lUV'''''U .... ,

nodular and nodular-mosaic bedded

antlVdlntc~s

Characteristic structures are:

H~'Jh~a~

OlOilarmnlanon, OC(:aSIOflall caJcifield

cy:an()tl~lctl:;mal1"' r "T ... 'nt ...

terLestra1e, deformation structures, and "' ...

'IJ .. ""L'-'

497

Nodules are several centimetres within the laminated nel,uu:-car- into red mudstones of the

2.1 m

J'1-:>u<'t1"'\n,"'<'

in more distal areas. Cons:ldenrlg

of the Zechstein basin

Arn1f'\T',>I""""r

of the PZ2 carbonates and in

MAIN ANHYDRITE A3

The " ...

.l1IJU"' ... d(~DOSlts

PZ3 are in the northern are 31.0 m thick. The 8-metre

from the upper of the is cornOletelV clC)mpol;ed

Fig. 3. Correlation Explanations in Table 1

L,V\,;IlMc:m Anhydrites in boreholes Tumlin PodgTOdzie IG 1 and Nieswin PIG 1

Koretacja poziomow anhydrytowych w o(wornch: Tumlin Podgrodzie IG 1 i Nieswin PIG I

1 - gipsy wt6rne, 2 ,:'Inl'1iV(I.""Vt" sz)deletowe, 3 - 4 - nnhydryty chnrlUr::Z:VS!:e. Jaminownne, - warstwowane.7 anhydryty i gruzlowo-mozaikowe, 9 - biolaminoidy, 10-iJowce, mulowce z siarczanami, 11 - dolomity z siarczanami, 12 interwaJ njerdzeniowany; pozostale objaSnienia w tabeli 1

m

km

A

Rudo Strawczynska 1

1

Tlr

Col

2

stachura 10 1

Tlr

rt Col Col

So bkho foci es:

Iv

^v

v vi

^{su I Dha} t e{1j ff..i,~ carbona te ~ sui phatel21

Salina lacies

IY\{YJ

16}

lithotypes I?f the Upper Anhydrite

5

JawOr2:na to 1 IG 1

rtr

T1r

Col Col

T1 T1

siliciclaslic -

rtr 11r

Col T1

E

A' 8

tqc:zna Zas'Z:osie IG 1

Tlr

carbonate -sillciclasticl41

c- :-:::1

siliciclastic [Sj

...,.

\0 co

Zechstein Anhydrites NW of the Cross Mts .... 499

"' ... ,rll.,.<+.,,"

which is a transitional facies between and halite rocks

This is because of abundant halite cement and the ImpOI'tarlce

"'V",'r'''''.TU

due to dissolution The rock is and crumbles when

",1'r.",,... ... 1\1

Impre~gnate:d

with halite. Halite are up to 2 in into

<lrl''"1U/,rllct=

host rock contaminated with dolomicrite

T"\r.'('",·r""'ri

pSelldc)moI1>hs after selenite are

"",...'"1"1'-'''''''

does not exceed 3.3 m in thickness and IG 1, Jaworze IG 1) above the conlposea of ""'"" ... ,." ... ,,

contaminated with material which occurs dls:perse:d

..,~" ... n,.."

diffuse and interbeds. Characteristic structures of are:

nr\filll'::.r

banded and nodular-mosaic. load structures, defonnation lami- peJlIW:-OOIC)mllt1C matrix and inter-

INTERPRETATION OF SEDIMENTARY ENVIRONMENT

A

Zechstein basin was determined salt and water and the

favoured continual free-flow water

_'''~''~'Ul-,~

between the shelf and the basin

centre. In the area north-west of the was related

) the Palaeozoic core of the Cross Mts.

Radom-Krasnik

These structural elements restricted sea-water incursions and affected the facies distribution Zechstein system of Wlldes,prc,ad SUlpnate

T'\1",trr,r""',"

and basins formed north-west of the Cross Mts. The

4. Stratigraphic-facies cross-section through the Zechstein Anhydrites along the line A Przekroj stratygraficzno-facjalny poziorn6w anhydrytowych cechszlyou wzdlut A - A'

Kompleks - facje: 1 siarczanowa, 2 - w<.;glanowo-siarczanowa, 3 4

wi;glanowo-silikoklastyczna, 5 6 - A-D litotypy gornego

500

OPOCZNO

WIERZ81CA

limit of the:

..A....il..A (1\

PZ2 Anhydrites Upper Anhydrite A1g .J...L...J... (41 Lower Anhydrite A1d

(5) Fault

• {61 borehole

Fig. Extent of the Zechstein Anhydrites in the area north-west of Ihe Holy Cross Mts.

Zasi~g poziom6w anhydrytowych cechsztynu w p6lnocno-zachodnim obrzezeniu

1 - znsj~g anhydrycu A3, 3 - zasi~g anhydrylu g6rnego A 19, 4 - zasi<;g

anhydrytu dotnego AId, 5 - uskok, 6

Zechstein NW of the Holy Cross Mts .... 501

top1oglrapntc co:ntlgUlraulon of the basement was the formation of the Zechstein The facies

more detailed reconstruction of sedllmentary the areas of the Zechstein basin COluplex de'/el()oe:Q in the perItidal

facies

rl";r",,,,c~lhl

delDO~)I

ts formed in subaerial settings and in ept1enn.eral

h'ype~rS~tl1nle

Characteristic structures are: nodules

and erosional dessication cracks. A stromatolitic and nodular facies

Qe'lfeliDDc~a

in shallow-water to subaerial en'If1f()nrnel1ts,

cleated selenites grew in stratified and a few metres

All these were incursions of sea-water as well as

brackish-water inflow runoff from the hinterland. Selenites characteristic mClrpJ101

I

o.e;lcalfonns:

ur~I'<':"_"1C

ITn ... u'''' ... r rh.rfHITrI'f't!

Tectonic-eustatic

sut)Sl{1ence,

nrl"l,rYlf'.r",rl

gralVHY-(;OIlllfCHle:Q basinward redistribution of clastic sul-

DIAGENESIS

, .. UUF>'-'J,''-'~J''-'

alterations which lead to

C. The effects of these

Preservation of structures and pSfmaomOllJhS fabrics of n"!1""Cn-ugypsum facies within the

""'~H1I'1""t.",..

was the main

basin.

II II II II II II II

II II II v II II

V V V II II II II II

II II II II

II II II II V ^{II II}

II II V II V

II

II

v

II II II V II

V II II II II II

II II V

V II II II

(0 siliciclastic - sulphate sabkha (2)

!5::$3_C01'bOl'loite -sulphate sebkha (3)

II II II II II V

II II V II II II

V II II II II II

V ^II

II v II II II II

II II II II V II

II II

.s

II~ II

II II II II II II

II II II II II V

II II V

II II II II II II II II

suI phate sabkha (4) shallow salina (5)

V

II

v

saliria Ilogoon

1

(6) borehole (1)

Zechstein Anhydrites NW of the Holy Cross MLS .... 503

EVOLUTION OF SEDIMENTATION

A eustatic in

movements and from increased

eV~lPOrat:LOn

of in the Zechstein basin studies show that the

de~)oSJ[tlOnal

ANHYDRITES

de[}OsltIc~n

of the Zechstein Limestone M.

led to the exposure and denudation of most of the

with

a

dominant continental

Se(llITlenltru-:v

Accretion of siliciclastic ael0mars

the

mosaic

<ln~"/rt"'ft"C'

PIG 1) AId section

.;)cnlagc~r,

H.

of sabkha-

Fig. 6. Facies and palaeogeography of the Zechstein Anhydrites (AI d, Al g, A2, and in the area north-west of the Holy Cross Mts.

J -9 - boreholes: J - Ruda Strawczynska 1, 2 Stachura IG 1, 3 - Cmitisk - Tumlin Podgrodzie 10 1, 5 Jaworzna IG

t.

6 - Goleniawy IG 1,7 -Jaworze IG

t.

8 -t.Oiczna ZllSzosie 10 PTG

Facje i poziorn6w anhydrytowych A2 i A3) w p6tnocno-zachodnim

obr:zeu!D!U G6r SWI~tOlcrz)'Ski~~h

obszary bez osad6w siarczanowych, 2 -sebha silikokla.styczno-siarczanowa, 3 - sebha wvglanowo-siar- czanowa, 4 - sebha siarczanowa, 5 - ptytJ.::a laguna, 6 -laguna, 7 - otw6r wiertniczy; 1-9 - nazwy otwor6w wiertniczych patrz tek.'>t angielski

504

~i)"'n~_.

_~/)

Alicja Kasprzyk

Fig. 7. Scheme of sedimentary environments of the Zechstein sulphate deposits in the area north-west of the Holy Cross Mts.

Schemat srodowisk sedymentacyjnych utwor6w siarcz.anowychcechsztynu w p6lnocno-zachodnim obrzeieniu G6r Swietokrzyskich

sulphate platforms and slopes in the peripheral parts of the Zechstein basin. Along with the progradation of sulphate platforms, formation of halite deposits of PZl started in rapidly subsiding local basins, presumably due to water-column stratification.

Further lowering of the sea level stopped the development of the sulphate platform and led to the exposure and intensive denudation of a large section of the southern region (Z.

Kowalczewski,

L.

Lenartowicz, 1975). The increased input of terrigenous material by torr'ential floods and streams from the hinterland resulted in the formation of a thick siliciclastic complex (Tl r) covering the sulphate deposits of the Lower Anhydrite or directly overlying the Zechstein Limestone (Fig. 4).

A marine transgression resulted in renewed evaporite accretion in the southern region, where a system of coastal flats developed early during the sulphate deposition of the Upper Anhydrite (Fig. 6). Only locally, in the extreme marginal areas, continuous siliciclastic deposition took place (M. Rup, 1985). The environmental system of the Upper Anhydrite comprised two main settings (Fig. 4): (1) sabkha-like coastal fiats, where different silici- clastic, carbonate and sulphate facies display a distinct lateral distribution, and (2) lagoons or salinas with continuous subaqueous sulphate deposition.

The sequence of the Upper Anhydrite in the north-west of the Holy Cross Mts. is

transgressive-regressive, similar to other areas in the peripheral parts of the Zechstein basin

(T. M. Peryt, 1990, 1991; A

.

Kasprzyk, 1992; T. M. Peryt, A. Kasprzyk, 1992). In the

southern region, breccias of BrA 1 (PI. T, Fig. 11) are thin or lacking. Where present they

are overlain by a platform sulphate facies (unit

C)

(Fig. 4; PI. I, Fig. 12). This succession

evidences the progressive sulphate deposition which, in the peripheral part of the evaporite

basin, took place along with transgression. Breccias formed during the flooding phase

following the sea level low stands, according to the model presented by B. W. Sellwood

Zechstein Anhydrites NW of the Holy Cross

Mes ....

505

for the Miocene of the Gulf of Suez. There are,

.... Alf-I1UHU'.lVJI.:ll

for the breccia formation in the

this will be the paper

the author.

Towards the end of the deIJOsltlcm of the southern in a coastal sabkha

PZ2 ANHYDRITES

favoured

",."",...,...,,-.t ..

pre:clrntatlOlrl.

was exposed and

Intl".n.;:nlPI"

aemlmlte(l,

1)

sedimentation took in ..

vl· ... " " "

A facies association expresses an unstable sedllmentary

VU111.I-"''-'''-

salina-sabkha system ae'veu)oe:a

level led to the

material in fluvial and

Fine differences in accretion and subsidence rate between the ...,,,, ... , ...

^'.>

more distal of the basin resulted in formation of a system of isolated

1'1", .... "''"'",,1, .... '''

1<"';;U'-Il'"

over a area of the northern where continuous sut)aque()us

ae{}OSltIa,n created a vast sulphate

nl!l,rTI'.rrn

Intense siliciclastic Series T2r started when in

climate and basin resulted in a brackish-water

inflow by runoff from the hinterland, The occurrence of facies of the ''',r",,,,",n ...

overlying the Series in the upper

PZ2

section

indicates renewed sea-water influx related with the initial of the PZ3

transj~reSslon.

PZ3 ANHYDRITES

In the southern region, of the Main where microbial and nodular facies ae'/el()oe:a environments of the

car'bonate-sul~)hate

material

terminates the sequence of the Zechstein Mts.

... '[Jr1T·' .. .".

was limited to areas,

... v1·.,."" ... "'I"

shallow-water to subaerial

reclepiOSJltlcin ofsiHciclastic

which

Cross

506

where a

Kowalczewski et

Alicja Kasprzyk

nrf'l,('fr'A,Ii!:lt-YAn

of the PZ4

CONCLUSIONS

sut)SI(lence, tectonic and eustatic

InrlUe~nc:mg

the short-term evolu- Z.

In

sea level fluctuations

resulted in In

variations. These were the main causes of pel'lptleral areas of the Zechstein basjn.

graltHl.lOe

to Doc. Dr. bab. LbJ[gnJlew Kowal-

n('r,,.·lnl"f

comments and remarks on earlier

versions of this paper. I also thank Stanistawa and Maria Kuleta M. for

Hanna Stec for the for hand

Oddziat SWilt;toikrz)tski

Panstwowego Instytutu Geologicznego Kielce, ul. Zgoda 21

Received: 24.05.1995

no. 6.20.1511.00.0.

REFERENCES

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KASPRZYK A. poz.iOtll0W anhydrytowych c.ec:11!':7Jvnll ol".n/kliJ1V Geo!., 40, p. 233-241, no. 4.

Prz.

Zechstein f\nnY(llll!~S NW of the Holy Cross Mts ....

507

KASPRZYK A.

l:'odgTollzle IG Kielce.

KENDALL A. C. (1992) - Evaporites and diagenesis; Quantitative diagenesis: Recent developments and applications to reservoir geology North Atlantic Organization (NATO), Advanced Study Institute, of Reading.

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t:waipOfltes and hydrocarbons (ed. B. C. Schreiber), p. Columbia Press. New York.

Z., LENARTOWICZ L. (1975) The Permian sequence in the north-western of the

Swi~tcJkrzyskie Mountains (in Polish with English summary). 19, p. 597-622, no.

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pOSZU}(lW.!ii rud Zn, Fe Arch. Panstw. Inst. GeoL

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508 Alicja Kasprzyk

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Alicja KASPRZYK

POZIOMY ANHYDRYTOWE CECHSZTYNU W NW OBRZEZENIU GOR SWmTOKRZYSKICH (GORNY PERM, CENTRALNA POLSKA): FACJE I PALEOGEOGRAFIA

Streszczenie

Obszar p6lnocno-zachodniego obrzezenia G6r Swivlokrzyskich wchodzi w sklad peryferyjnej cZc;Sci zbiof- nika cechsztynskiego (fig. 1), co znajduje odzwierciedlenie w niepetnym rozwoju sedymcntacji cyklicznej utwor6w ewaporatowych cyklotem6w PZl. PZ2, PZ3 i PZ4 oraz duzym udziaLe skat klastycznych (fig. 2, tab. 1).

Analiza wyksztalcenia litofacjalnego poziomow anhydrytowych w wybranych otworach wiertniczych pozwala wyr6znic dwa 0 nieeo odmiennym wyksztaiceniu utworOw cechsztynskich i

procesie potudniowy (tzw. bhskie obrzeZenie pe(111Sko-mezozoiczne Gar SW'ictokl"Zyskich) p6tnocny (tzw. obrzezenie dalekie) (fig. 2,3).

W obrzei:eniu bliskim anhydryt dolny jest wykszta1cony jedynie lokalnie jako anhydryty gruzlowe i gruzlo- wo-mozaikowe. powstale w srodowisku sebhy. Sekwencja anhydrytu g6mego obejmuje eztery Iitotypy (fig. 4).

Rozpoczynajlt jq. i10wce i mufowee, lokalnie skaly wr;glanowe z siarczanami, lub utwory siarczanowe silnle zanieczyszczone. leh rozw6j, zwiq,zany z nOWq objqt slrefe brzeznq zbiornika. Wyzej w profil u wyst~puj<l brekcje anhydrytowo-ilaste, a ponad gruby kompleks anhydryt6w i gips6w wt6mych masywnych i mozaikowych. Utwory te w ~rodowisku prytkich, potqczonych Iaglln (salin), tworzilcych system platformy siarczanowej. an hydrytu g6rnego koficZil osady siarcz.anowo-w~glanowo-si Ii koklastyczne o teksturach Rozw6j ich zachodzil w warunkach cz~stych zmian rezimu fizykochemicznego, sebhy paralicznej. Tym samym sekwencja anhydrytu g6mego w p6lnocno-zachodnim obrzeieniu G6r rna charakter transgresywno-regre- sywny.

Na obszarze dalekiego obrteienia permsko-mezozoicznego G6r utwory siarc7..anowe PZI reprezentujll facje platformy sinrczanowej i jej sklonu. W czasie rozwoju anhydryt6w gnlZt()WID-nr102~aHco\:vyc:h cyklu PZ2 w srodowisku sebhy, rozwini~tej w dalekim obrzeieoill G6r strefa obe~Jmujqca lJbszar ('\hl-7f',~1f',ni~ bliskiego - byla wynuc>.:Ona i poddana intensywnej denudacji. Utwory siarczanowe poziomu A2r to osady inicjaInej tf1lnsgresji cyklu PZ3, kt6ra objvtll swym zasi~giem jedynie obrzeienie daIekie (fig. 5). Na obszarze tym ulwory siarcZ<l.nowe anhydrytu gt6wnego S4 wyksztakone jako anhydryty gruzlowe - w cZI,(Sci dolnej, oraz utwory siarczanowe laminowane i gruzlowo-mozaikowe - wyiej.

Utwory te powi\ta!y w srodowisku skrajnie piytkowodnym i subaeralnym systemu sebhy weglanowo-siarczanowej (fig. 6). W tym czasie w dalekim obrzezeniu G6r Swi~tokrzyskich !:\vorzyIy siv w zbiomiku

selenitowe, kt6rych charakterystyczne struktury krystaliczne dzis Sq Ulchowane w anhydrytach sz~:je!elciw~lch formie pseudomorfoz.

Zechstein Anhydrites NW of the Holy Cross Mts ....

509

Na~lpelnif!Js2~ wyksztakenie i najsrerszy (fig. 2, 5). Duze zrowico-

wlllnlel1t()ta¹cJalne oraz bogaty inwentarz siarczanowych (tabl.

r,

fig. 8-14) wskazujQ na zmienne warunki sedymentacji. Warunki te, zrekonstruowane na podstawie analogii do wsp6tczes- nych srodowisk ewaporacyjnych, srodowiska zar6wno subakwalne (wzgl~dnie gl~bokowodne i plytkowodne), jak i subaeralne (fig. 7).

Fig. 8. NOlilutar-lnO!:mc aflrlYUnlt~ W:IUl ,QU10Jfme

depth 376.8-377.0

rn

PLATE I

gruzlowo-mozaikowy 0 matriks dolomitowym, gesto zylkowany gipsem wlOknistym; anhydryt dolny;

(bil:>pelmicrc)sp,arite) irregularly laminated, with sulphate nodules and impregnations. and with (dark) are distorted by sulphate nodules resembling pseudomorphs after gypsum crystals (arrows); Lower Anhydrite; depth 379.65-379.80 m

Biopelmikrosparyt nieregularnie laminowany z impregnacjami siarczanowymi, g(:sto zyikowany gipsem; laminy iIasto-organiczne (ciemne) przebiegu zatlUrlWnym

379,65-379,80 m

10. Graded-bedded with erosional base at the contact with mosaic anhydrite (lower part); Lower

AnnV(ln[,e: depth m

fmkcjonalnie warstwowany, w dole ostro kontaktujq.cy

z

anhydrytem mozaikowym; anhydryt dolny;

oriented lInifnrTrlI·v·

B rekcja anllVdlrvt:ow'o-llasta (D) i

sktadniki wykazuj!\. jednokierunkowfl orientacj~;

1943,4-1943,5

m

orf~nnicznq; wydlutooe litotyp B; g!eb.

Fig. 12. Mosaic anhydrite note relicts of regular growth bands of former gypsum prisms (arrows); Upper unit C; depth 343.20-343.35 m

Anhydryt mozaikowy z pseudomorfozami po witlZkach se!enitowych typu cavoli; miejscowo czytelne relikty stref pierwotnych kryszta16w pryzmatycznych gipsu (strzalki); anhydryt g6rny, Iitotyp C; gteb. 343,20-

m

Fig. 13. Nodular-mosaic bedded anhydrite with alternation of layers: anhydrite (A) and dolomitic siltstone (D);

small arcuate-shaped nodules are anhydrite pseudomorphs after prismatic gypsum crystals; Basal Anhydrite; depth 1894.65

na~,rze:mi,:mlc~gl),mlwarst\warm atlhydrytu (A) i mulowcadolomi- o zarysach ostro}cra1Ne(izi~;ty(~h pseudomorfozy 'lnh,\II1,·ut .. po krysztatach pryzma- podstawowy; gieb. 1894,65 m

anl1lydl1te; pseudomorphs after crystals outlined by aOlOm!lte··on~anIC material;

dis:sollJtjOlfi pores after Main Anhydrite; depth 1868.40-1868.55 m

Anhydryt szkie1etowy; zarysy pseudomorfoz po krysztalach selenitowych podkr~lone ciemnymi smugami dolomitowo-organicznymi; liczne pory z rozpuszczania anhydryt gf6wny; gl~b. 1868,40-1868,55 m Figs. 8,9,12 Tumlin Podgrodzie IG I borehOle; Figs. 10, 11, 13.14- NieSwifi PIG 1 borehole

Fig. 8, 9, 12- otw6rwiertniczy Tumlin Podgrodzie IG l; fig. [0, 11. 13, 14- otw6r wiertniczy Nieswifi PIG [

Geo!. Quart. No.4, 1995 PLATE I

Alicja KASPRZYK - Zechstein Anhydrites NW of the Holy Cross Mts. (Upper Permian. central Poland): facies and palaeogeography