Carboniferous palynostratigraphy of Polish Coals Basins

nego. Utwory barrandienu w Masywie Czeskim zinter-pretowano jako osady morza marginalnego oddzielonego od otwartego oceanu łukiem wysp, którego fragment ciągnie się od metamorfiku kłodzkiego po blok karkonosko--łużycki. W turneju i namurze A miały miejsce kolejne

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HALINA KMIECIK

Instytut Geologiczny

CARBONIFEROUS PALYNOSTRATIGRAPHY OF POLISH COALS BASINS

Carboniferous coal basins of Poland (Fig. 1) originated during evolution of Variscan geosynclinal system and adjacent platform areas (12). The Lower Silesian Coal Basin (LSCB) originated as intramontane depression, the Upper Silesia Coal Basin (USCB) was a part of foredeep molasse, while the Lublin Coal Basin (LCB) originated within the East European Platform due to diff erential movements of the basement. The stratigraphic successions of these coal basins are differentiated and span the Upper Visean through Stephanian.

Intensive biostratigraphic research in the Polish coal basins has been carried out from many decades, whereas the history of palynological investigations, particulary those based on miospores, comprises the last 30 years. These investigations were initiated and are continued in the USCB by A. Jachowicz (1956-1972), S. Dybova and A. Jachowicz (1956-1968) and by other workers. Detailed data on the history of spore research and the full bibliography for this time periods are given by A. Jachowicz (7). The most importand outcome of this re-search was the recognition of a large number of Carboni-ferous miospore taxons and the microfloral zonation of coal-bearing deposits in the USCB.

Microfloral investigations in the LCB date back to the discovery of the Carboniferous deposits in the area, whereas a systematic and intensive miospore research began here in early nineteen-sixties of the present cen tury and progressed in accordance with the advances of local Carboniferous geology (A. Jachowicz 6, H. Kmiecik -8-10). The results of microfloral investigations in the LSCB are included mainly in publications by T. Górecka (2, 3) and H. Krawczyńska-Grocholska (13, 14).

The purpose of the present paper is (1) to summarize the results of palynological research carried out to data in the Carboniferous of Polish coal basins (2) to correlate palynological zonal schemes of these basins, and (3) to establish the palynostratigraphic correlation between the Polish and West European Carboniferous coal basins.

UKD 561 :581.33] :551.735.02: 553.94(438)

CARBONIFEROUS MIOSPORE STRA TIGRAPHY IN POLISH COAL BASINS

The miospore zonal schemes of the Polish Carbonifer-ous coal basins, as given below, are based mainly on the present author's work in the Upper Silesian and Lublin

Fig. 1. Location of the Carboniferous coal basins in Poland - extent of the Carboniferous in Poland, 2 - margin of the • East-European Platform, LSCB - Lower Silesia Coal Basin, USCB - Upper Silesia Coal Basin, LCB - Lublin Coal Basin

Ryc. 1. Położenie karbońskich zagłębi węglowych w Polsce 1 - zasięg karbonu w Polsce, 2 - brzeg platformy wschodnio-europejskiej, LSCB - Dolnośląskie Zagłębie Węglowe, USCB

-Górnośląskie Zagłębie Węglowe, . LCB - Lubelskie Zagłębie Węglowe

UPPER SILESIA COAL BASIN

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STEPH. KWACZAŁA ARKOSE

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Fig. 2. Distribution of stratigraphically significant miospore species in the Carboniferous deposits of the Upper Silesia Coal Basin

Coal Basins. The relevant data for the Lower Silesia Coal Basin were summarized from the literature (Figs 2, 3 and 4).

Upper Silesia Coal Basin

In the past decade,' 20 deep wells were drilled of in the USCB in order to penetrate the deep levels of the coal--bearing succession. The wells were located within the entire basin, particularly in areas of poor recognition. A remarkable advantage of these wells was full coring and, in most instances, nearly full core recovery. The cores

248

yielded and unique midspore materiał from the whole profile of the Upper Silesia Carboniferous. The miospore research was concerned on all coal seams and coaly inter-calations, as well as on a number of samples of barren rocks, penetrated by the wells. For the first time, excellently preserved miospores were received from the lowest part of the profile, including carbonate rocks, the entire s~ction of the Malinowice/Zalas Beds and the basal part of the

parallic deposits (Samow Beds). The results of the miospore research were used for erection of a synthetic palynostrati-graphic subdivision of the Carboniferous in the USCB (Fig. 2).

zone of maximum presence zone of reduced presence

405 - coat beds number

VII - faunistic horizon

Ryc. 2. Rozmieszczenie stratygraficzne ważnych gatunków miospor w utworach 'karbonu Górnośląskiego Zagłębia Węglowego The complete of the Upper Silesia Carboniferous

comprises the deposits ranging in age from the latest Tournaisian (?)-early Visean till Stephanian. In the profile, 14 miospore zones were distinguished, 2 in the Dinantian and 12 in the Silesian. This miospore zonal scheme was compared with the lithostratigraphic standard for the area and the age designation of the miospore zones was established.

Lower Silesia Coal Basin

Palynostratigraphic investigations are important in

the LSCB because of the limnic nature of the Silesian in this region. However, the present state of palynological resolution of the Lower Silesia Carboniferous remains still unsatisfactory. Most camplete palynological documen-tations were obtained for the Wałbrzych Formation, Biały Kamień Beds and for the barren deposits of the uppermost Carboniferous (Upper Westphalian - Stephanian). These data are supplemented by the valuable paper by M. Kaise-rova-Kalibova (17), concerning the palynostratigraphy of the Westphalian and Stephanian in the Bóhemian part of the basin.

LOWER SILESIA COAL BASIN

P RHIAN z

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LITHOSTRATl-GRAPHY

(A.Grocholski; 1981, 1983) LUDWIKOWICE Fm. ~ - ŁOMNICA Mb. ~ B LU ~ GRZMIĄCA Mb.

PALYNOSTRATl-GRAPHY

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Fig. 3. Distribution of stratigraphically significant miospore species in the Lower Silesia Coal Basin

in the Carboniferous of the LSCB, presented in Fig. 3, are given after the publications listed above, and from contributory notes. These ranges are here set in order and placed within the lithostratigraphic standard of the LSCB. In this standard, 10 miospore zones were distinguish-ed, spanning the Namurian A through Stephanian.

Deposits older than the Namurian were searched for microflora by H. Krawczyńska-Grocholska (14) in the Świebodzice Depression. A mixed Devonian-Early Carboni-ferous spore assembl<:1.ge, identified there, was probably formed due to a late Visean redeposition.

Lublin Coal Basin

In the past two decades the palynological investigations in the Carboniferous of the Lublin Coal Basin were intensi-vely carried basing on materials from number of wells with coring and nearly full core recovery. They were con-centrated mainly on coal seams and coaly intercalation, but also on samples taken from barren intervals. The results of miospore research provided the basis for the erection of a palynostratigraphic zonal scheme in the profile ranging in age from the late Visean till the West-phalian D. In this profile, 13 spore zones were distinguish-ed (Fig. 4).

250

CORRELATION OF CARBONIFEROUS PALYNOSTRATIGRAPHIC SCHEMES

IN POLISH COAL BASINS

Carboniferous spore subdivisions of different coal basins were compared through relating them to the chrono-stratigraphic standard (Fig. 5). In this way, correlation was made between miospore zones of all three coal basins. The comparison of stratigraphic ranges of the diagnostic taxones and those characteristic of local spore subdivisions permitted to select those taxons which can be considered as diagnostic for a synthetic miospore scheme valid for all Polish basins. In identified spore zones, these taxons form characteristic assemblages of genera and species. This synthetic scheme comprises the deposits spanning the late Tournaisian-early Visean (?) through the Stephanian and includes 14 miospore zones.

Verrucosisporites nitidus-Lycospora pusilla (NP) Miospore Zone

This zone was identified in the carbonate deposits of the USCB. The sporomorphs, found recently here, indicate an early Visean (?), possibly ·'-also late Tournaisian-early Visean (Tn₃ - V₁_₂) age of these deposits. The Visean age

I -

zone of maximum presence I

I - zone of re_duced presence

I

111

Ryc. 3. Rozmieszczenie stratygraficzne ważnych gatunków miospor

w Dolnośląskim Zagłębiu Węglowym

is suggested by the presence of the species Lycospora pusilla (Ibrahim) Somers, Lycospora noctuina Butterworth et Williams, Verrucosisporites nitidus (Naumova) Playford and fragments of Tripartites sp. The spore assemblage is relatively rich. It is possible that some sporomorphs were redeposited from older sediments (Devonian ?). The final age assignement of the NP Zone must await a comparison with faunistic evidence.

The boundaries of the NP Zone are not yet defined precisely. The upper boundary is erosive.

Murospora aurita- Diatomozonotriletes saetosus (AS) Miospore Zone

The AS Zone was identified in the USCB and LCB. In the USCB it comprises the lower part of the marine--diastrophic deposits (lower part of the Malinowice/Zalas Formation), while in the LCB it corresponds in a Carbonate--Clay "series" (Huczwa Formation). In both coal basins the lower limit of the AS Zone corresponds to the base of the Carboniferous paleontologically documented. The upper limit of the zone is set up by the disapearrance of numerous taxons characteristic only this zone, including the index taxon Murospora aurita (Waltz) Playford (in both coal basins) and Diatomozonotriletes saetosus (Hac-quebard et Barss) Hughes et Playford {in LCB).

The AS Zone corresponds to late Visean (V

:J,

goniatite P1 (a part ?) and P2 zones.

Tripartites rugosus- Diatomozonotriletes ubertus (RU) Miospore Zone

The RU Zone was distinguished in all three coal basins. In the USCB it corresponds in the three succesive local zones Tb, Pp and Ti, all having the features typical of the RU Zone.

The base of the RU Zone is defined by the absence of relatively numerous Early Carboniferous taxons, and the first appearance of, still rare, younger species, such as

Punctatisporites sinuatus (Artiiz) Neves, Crassispora

ko-sankei (Potonie et Kremp) Bharadwaj, Laevigatosporites

spp. and others. The upper limit of the zone is indicated by the sudden decline of the genus Triparites, which is abundant in the RU Zone together with

Diatomozono-triletes, Pseudoannulatisporites and some species of

Chaeto-sphaerites and Rotaspora.

In the USCB the RU Zone corresponds to the upper part of the marine-diastrophic deposits (upper part of the Malinowice/Zalas Formation) and to the lower part of parallic deposits runging up to the faunistic horizon VII (Enna). In the LSCB the zone includes the lower part of the Wałbrzych Formation, in the LCB - the Komarow Beds (except their uppermost segment) from the limestone A to a level between the limestones G and H.

The RU Zone corresponds to the early Namurian A (E₁ and lower Ez goniatite zones).

Chaetosphaerites pollenisimilis- Rotaspora knoxi (PK) Miospore Zone

The PK Zone was distinguished in all three coal basins. lts lower limit is established by the abrupt decline of many Early Carboniferous-early Namurian taxons. Its upper limit is set up by finał disappearrance of last, older species which in a relic form continue form lower zones, for in-stance such index species as Chaetosphaerites

pollenisi-milis (Horst) Butterworth et Williams and Rotaspora knoxi

Butterwoth et Williams, and others.

In the USCB the PK Zone comprises an interval rang-ing from the faunistic horizon VII (Enna) to the base of the coal seam 51 O. In the LSCB it includes the topmost part of the Wałbrzych Formation, while in the LCB the uppermost Komarów Beds and a lower part of the Bug Beds, including the limestone I. The upper limit of the zone is erosional in the USCB and LSCB.

In the chronostratigraphic standard the PK Zone corresponds to the late Namurian A, ie„ upper part of the Ez goniatite zone and possibly equivalents of the H zone.

Densosporites variabilis- Reticulatisporites carnosus (VC) Miospore Zone

The VC Zone was established in the USCB and LCB, while it is lacking in the LSCB (stratigraphic hiatus). This zone is characterized by the qualitative impoverish-ment of spore assemblage, lack of most Early Carboni-ferous-early Namurian taxons, onset of single miospore

specimens representing species typical of the Westphalian, and by either the marked quantitative dominance of the genus Densosporites and related forms (in the USCB) or the increased content of these genera (in the LCB).

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---CH RONOSTRATIGRAPHY LITHOSTRATIG RA PHY };? ~~ :::o :z l> o " V') :I: -ł -< :::o ~ I Murospora aurita Murospora tripulvinata Murospora margodentata Procoronaspora ambigua Oiatomozonotriletes saetosus Stenozonotri letes c Ian.is Corbulispora cancellata Oiatomozonotri letes ubertus Tripartites incisotrilobus Anapiculatisporites serratus Murospora . sublobata Auroraspora solisortus Tripartites rugosus Triquitrites trivalvis l e:: c::c

c

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c::c )> V') :z Rotaspora annelitus Pseudoannulatisporites polonicus Schulzospora primigenia Discernisporites micromanifestus Chaetosphaerites variabilis Rotaspora fracta Schulzospora elongata Rotaspora knoxi Chaetospha~rites pollenisimilis Anapiculatisporites hispidus Remysporites magnificus Schulzospora ocellata Tri partites spp. Reticulatisporites carnosus Bellispores nitidus L ycospora n octu ina Schulzospora rara Punctatisporites sinuatus Crassispora kosankei Ahrens1sporites guerickei Laevigatosporites spp. Florinites spp. Radiizonates difformis Raistrickia fulva Grumosisporites varioreticulatus Alatisporites pustulatus Rad ii zonates a ligerens

I I I I I I I . I I I I I I I I I I I I _I I _I I _I I I I I

- zone of maximum presence

zone of reduced presence

380 - coal beds number

S - key limestone beds

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I I I I I I I I I I I I

Ryc. 4. Rozmieszczenie stratygraficzne ważnych gatunków miospor

w utworach karbonu Lubelskiego Zagłębia Węglowego

in the LSCB, except their topmost part, up to the base

of the limestone M.

The VC Zone corresponds to the Namurian B (R

goniatite zone).

Grumosisporites varioreticulatus-Cingulizonates

loricatus (VL) Miospore Zone

The VL Zone was identified in the USCB and LCB,

whereas in the LSCB the deposits corresponding to the

upper part of the zone were reported. The lower limit of the zone is indicated by the onset or regular occurrence of the species Grumosisporites varioreticulatus (Naves) Smith et Butterworth, Cingulizonates loricatus (Loose) But-terworth et al., and other species which occur sporadically

in the highest part of the preceding zone and, from the

base of the VI Zone, they appear regularly upwards. Up

section there is a systematic younging of the miospore

assemblage.

In the USCB the VL Zone includes the Ruda Beds

(from the top of the coal seam 501 to a faunistic horizon in

the vicinity of the seam 407). In the LCB this zone comprises

the topmost part of the Bug Beds and the lower portion

of the Kumow Beds, up to the bottom of the limestone P.

In the LSCB the zone should include a lower part of the

Biały Kamień Beds, equivalent to the highest part of

the VL Zone, which occur above a hiatus spanning much

of the late Namurian in this basin.

The VL Zone corresponds to the Namurian C (G₁

goniatite zone).

Lycospora punctata- Raistrickia fulva (PF)

Miospore Zone

The PF Zone has equivalents in all three coal basins.

It is defined by the regular occurrence of relatively

abun-dant sporomorphs characteristic of the Westphalian and

the relic occurrence of some Namurian species, such as

Schulzospora rara Kosanke, Bellispores nitidus (Horst) Sullivan, Punctatisporites sinuatus (Arti.iz) Neves,

Lyco-spora noctuina Butterworth et Williams, and others, as

well as by the appearrance of single specimens of Lycospora

punctata Kosanke and L. pusilla (Ibrahim) Somers. In the

USCB the PF Zone contains, in addition, also numerous

Densosporites and related genera.

In the USCB the PF Zone corresponds to a lower part

of the Zaleze Beds, up to a level near the coal seam 401,

in the LCB - a middle part of the Kumow Beds, and in

the LSCB - an upper part of the Biały Kamień Beds.

In the chronostratigraphic terms the PF Zone spans

a lower part of the Westphalian A, essentially up to the top

of the Lenisulcata chronozone.

Radiizonates aligerens-Schulzospora rara (AR)

Miospore Zone

The AR Zone is identified in all three coal basins. In

the USCB and LCB this is the acme zone of Radiizonates

aligerens (Knox) Staplin et Jansonius. In addition, in all those basins, the last numerous occurrence of the species

Punctatisporites sinuatus (Artiiz) Neves and Schulzospora

rara Kosanke is recorded from this zone. The spore assem-blage of the AR Zone is rich in species and, in most

instan-ces, is characterized by the regular occurrence of taxons

typical of the Westphalian, as well as by the marked

in-crease in abundance of the genera Grassispora,

Laevigato-sporites, Florinites and others. Near the top of the zone, there appear sporadically some taxons characteristic of

upper Westphalian.

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13

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Fig. 5. Palynostratigraphic correlation of the miospore zonations in coal basins in Poland part of the Zaleze Beds (from the seam 401 to the vicinity

of seam 327), in the LCB ~ an upper of the Kumow Beds and the lowest part of the Lublin Beds, up to a level of the limestone S, and in the LSCB - a middle part of the Zader Formation (Boguszow Member).

The age of the AB Zone was determined as the late Westphalian A (Communis chronozone and lower part

of Modiolaris zone).

Endosporites globoformis-Dictyotriletes bireticulatus (GB) Miospore Zone

The GB Zone was distinguished in all three basins. 254

In the USCB and LCB it also includes local miospore zones, Ts and Vm, which correspond the uppermost part of the generalized GB Zone.

The base of the GB Zone is defines by regular and usually common occurrences of the index species

Endo-sporżtes globiformis (Ibrahim). Smith et Butterworth and

Dictyotriletes bireticulatus (Ibrahim) Smith et Butterworth,

along with other spores which appear or occur regularly upward from the base of the GB Zone. This base is also indicated by the extinction of Radiizonates aligerens (Knox)

Staplin et Jansonius, with the exception of the USCB where it is recorded sporadically in this zone. The upper limit of the zone is indicated by the decline of some older

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MIOSPORE ZONATION

THE

CARBONIFEROUS DEPOSITS

IN THE

POLISH COAL

BASINS

SM An~ulisporites splendidus Cad1ospora magna LU Sp.e~iososp~rites laevigatus lll in1tes unicus GT Lundb~andis.pora gigantea

Latensina tri teta

OE Thymospora obsc:ura Triquitrites exiguus S Torispora securis F Vestispora fenestrata Endosporites globiformis GB Oictyotriletes bireticulatus AR Radiizonates aligerens Schulzospora rara Lycospora punctata PF Raistrickia fulva 2 I

r1

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I 1 li I I _I 11 I 2 1• _I 1 I 2 I ₃ I I 11 1 2 3 1 3 Oensosporites variabilis VC Reticulatisporites carnosus Chaetosphaerites polleni si mi I is PK Rotaspora knoxi

1 - Upper Silesia (oal Basin 2 - Lublin Coal Basin

3 - Lower Silesia Coal Basin RU Tripartites rugosus Oiatomozonotriletes ubertus

I

-

zone of maximum presence I

I - zone of reduced presence

Murospora aurita

I

AS Oiatomozonotriletes saetosus NP Verrucos1sporites nit1dus

Lycospora pusilla

Ryc. 5. Korelacja palinostratygraficzna zonacji miosporowych zagłębi węglowych w Polsce

species, such as Bellispores nitidus (Horst) Sullivan,

Puncta-tisporites sinuatus (Artiiz) Neves, Raistrickia fulva Artiiz,

Grumosisporites varioreticulatus (Neves) Smith et

Butter-worth, and other species, as well as by the onset _of some miospores characteristic of the ·late Westphalian.

In the USCB the GB Zone include the Orzesze Beds together with a lower part of the Laziska Beds, in the LCB - a part of the Lublin Beds from the limestone S to the co al seam 369, and in the LSCB - an upper part of the Zader Formation (Gorce Member).

The miospore GB Zone corresponds to the Westphalian B, i.e., upper ,part of the Modiolaris chronozone - lower part of the Similis-Pulchra zone.

Torispora securis-Vestispora fenestra (SF)

Miospore Zone

The miospore SF Zone was identified in all three basins. In the LCB it corresponds to two local zones, Vm and Vf. The base of the SF Zone is indicated by the appearrance of taxons typical of the late Westphalian, such as the index species Torispora securis (Balme) Alpem, Doubinger 1et

Horst, Vestispora fenestrata (Kosanke et Brokwa) Spode

and, among others, Torispora laevigata Bharadwaj,

West-phalensisporites irregularis Alpem, Punctatosporites granifer

Potonie et Kremp, Triquitrites bransoni Wilson et Hoffmei-ster. The top of the zone is indicated by the gradual decline

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Westphalensisporites irregularis Oisaccites non striatiti Microreticulatisporites nobilis Florinites junior Vestispora fenestrata Torispora spp. Oisaccites striatiti Lundblandispora gigantea Potoni~isporites spp. Latensina spp. Thymospora spp . Spinosporites spinosus Polymorphisporites spp . Angulisporites splendidus

Fig. 6. Stratigraphic distribution of certain selected miospore species in the Carboniferous deposits of Western Europe and the coal basins

· in Poland

Ryc. 6. Rozmieszczenie stratygraficzne pewnych wybranych ga-tunków miospor w utworach karbonu zachodniej Europy i zagłębi

węglowych w Polsce .

or quantitative reduction of some taxons, such as Dictyo-triletes bireticulatus (Ibrahim) Smith and Butterworth, Radiizonates spp„ Vestispora spp., and the appearrance

of sporomorphs characteristic of the Westphalian and Stephanian.

In the USCB the SF Zone comprises an upper part of the Laziska Beds, in the LSCB - a lower part of the Glinik Formation, and in the LCB - an upper part of the Magnuszew Formation. The upper boundary of the zone in the LCB is not fixed firmly as yet.

256

The SF Zone corresponds to the Westphalian C (upper part of the Similis-Pulchra zone and the Phillipsii zone).

Thymospora obscura-Triquitrites exiguus (OE) Miospore Zone

The OE Zone was identified in all three coal basins, although in each of them diff erent parts of the zone are probably present. This is shown by differences in the ranges of the index and characteristic taxons. In the LCB probably

a lower part of the OE Zone occurs, as is suggested by the lack of the majority of miospores characteristic of the latest Westphalian and the Stephanian. In this basin the boundaries of the OE Zone are provisionally set up, due to scarcity of suitable sections. In the LSCB, the spore assemblage of the CE zone is typical of the late West-phalian, although it lacks most of the species characteristic of the latest Westphalian and the Stephanian, which in this basin appear in a higher zone. In the USCB the miospore assemblage of the OE Zone contains species characteristic of the latest Carboniferous, thus, it is the youngest among

those assemblages. lt is likely that in the USCB only an

upper part of the OE Zone is represented, while its lower

part falls within a stratigraphic hiatus. On the other hand,

these differences may be facies controlled.

In the LSCB the OE ,Zone includes a higher part of the

Glinik Formation, in the USCB - the Libiaz Beds, and

in the LCB - an upper part of the Magnuszew Formation. The OE Zone corresponds to the Westphalian D (Tenuis chronozone).

Lundblandispora gigantea-Latensina trileta (GT) Miospore Zone

The GT Zone and higher zones were identified only in the LSCB, because palynologically dated deposits of

a Stephanian ,age occur only in that basin. The deposits

assigned to the Stephanian in the USCB (Kwaczala arkose)

contain only single specimens of long-ranging microflora which has little stratigraphic value.

The GT Zone is defines by the disappearrance of most taxons characteristic of the W estphalian and by the onset

of forms typical of the Stephanian, such as Lundblandispora

gigantea (Alpem) Doubinger, Latensina trileta Alpem, and others, in the LSCB the GT Zone was distinguished in the upper part of the Glinik Formation (upper part of

the Grzmiaca Member). lt is probably equivalent to the

early Stephanian (A - B ?) in the Carboniferous chrono-stratigraphic standard.

Speciososporites laevigatus-Illinites unicus (LU) Miospore Zone

The LU Zone is typified by the absence of some taxones of the latest Westphalian and the early Stephanian, and by the appearance of new species, such as Speciososporites

laevigatus Alpem, Potonieisporites spp. and first occurrences of Disaccites striatiti.

In the LSCB the LU Zone comprises the highest part of the Glinik Formation (Lomnica Member) and it pro-bably corresponds to the late Stephanian (B?-early C?).

Angulisporites splendidus-Cadiospora magna (SM) Miospore Zone

The SM Zone, identified in the LSCB, is characterized

by the onset of the index species Angulisporites splendidus

Bharadwaj and Cadiospora magna Kosanke. ·

This zone was distinguished in the Ludwikowice Forma-tion and corresponds to the latest Stephanian (C?) and earliest Permian.

COMPARISON OF CARBONIFEROUS PALYNOSTRATIGRAPHIC SCHEME OF POLISH

COAL BASINS WITH CARBONIFEROUS MIOSPORE ZONA TION OF WEST EUROPE The synthetic palynostratigraphic scheme erected for the Carboniferous coal basins of Poland provides a basis

for the inclusion of Polish data to united palynostratigraphic classification of the West European Carboniferous, proposed by the Commission Internationale de Microflore du Paleo-zoique (G. Clayton et al, 1). The juxtaposition of the

strati-graphic ranges of diagnostic taxons in the West European

scheme with the ranges of the same miospores in the Polish

Carboniferous coal basins (Fig. 6) points to a remarkable

convergence of criteria used for the erection of both schemes and to identity, or great similarity, in the miospore zones identified in both areas.

The diff erences in occurrence and ranges of some taxons, thought to be the index ones for particular sec-tions of the Carboniferous in different coal basins, may be related to development of the coeval deposits in different facies, which gave rise to a growth of flora in variable ecological conditions. The above considerations support the notion on the existence of a large number of index taxons and characteristic miospore assemblages, which permit a very detailed age correlation to be made between distant Carboniferous successions development in the same palaeo-floral province.

Translated by S. Porębski

REFERENCES

1. C 1 a y to n G„ Co q u e 1 R. et al. - Carboniferous spores of western Europe: illustration and zonation.

Meded. Rijks Geol. Dienst. 1977 vol. 29.

2. G ó r e c k a T. - Stratigraphy of the Biały Kamień

Beds in the north-western part of the intra-Sudetic

trough on the ground of palynological researches.

Biul. Inst. Geol. 1969 230.

3. G ó re c k a T. - Results of palynostratigraphic tests

of the youngest Carbonif ero us formation in the Low er

Silesian Region. Prace Nauk. Inst. Górn. Politechn.

Wrocł., nr 40, Monografie 1981 nr 19.

4. Gr och o 1 ski A. - Propozycja podziału silezu na

formalne jednostki litostratygraficzne w polskiej części

depresji śródsudeckiej. Materiały IV Symp. Geol.

form. węglon. Polski, Kraków 1981.

5. Gr och o 1 ski A. - The Carboniferous in

south-western Poland. Prz. Geol. 1983 nr 6.

6. J a c h o w i c z A. - Microfloristic characteristics of

the deposits of the Lublin Carboniferous. Prace Inst.

Geol. 1966, vol. 44.

7. Jach o w i cz A. - A microfloristic description and

stratigraphy of the productive Carboniferous of the Upper Silesian coal basin. Ibidem 1972 vol. 61.

8. K m i e c i k H. - Spore stratigraphy of

central--eastern Poland. Ann. Soc. Geol. Pol. 1978 vol. 4,

z. 3-4.

9. Kmiecik H. - Palynostratigraphy of the Lublin

Coal Basin. In: Geological Problems of coal basins in Poland. Geological Institute, 1983.

1 O. Km i e c i k H. - Palynostratigraphy of the Carboni-ferous at the margin of the Polish part of the East--European platform. Rev. Palaeobot. Palynol. 1986

vol. 48.

11. Kot as A. - Structural evolution of the Upper Silesian Coal Basin (Poland). C.R. Dix. Congr. Int. Strat. Geol. Carbonif., Madrid 1983, 1985, vol. 3.

12. Kot as A., Porzycki J. - Major features of

Carboniferous coal basins in Poland. Prz. Geol.

1984 nr 5.

13. K r a w c z y ń s k a - Gr o c h o 1 s k a H. - Le

Na-murian du Bassin de Nowa Ruda a la lumiere des

14. K r a w c z y ń s k a - G r o c h o l s k a H. - Sporo-morph assemblage in sandstone and siltstone samples from Chwaliszów in the Świebodzice depression (Cen-tral Sudetes). Biul. Inst. Geol. 1973, 264.

15. Porzycki J. - Fundamental properties of the geological structure and evaluation of the deposits of the Lublin coal basin. Ibidem 1980, 328, 9eology of Poland vol. Ili.

16. P r a c a zbiorowa - Karbon Górnośląskiego Zagłę­

bia Węglowego. Prace Inst. Geol., 1972, v. 61.

17. T

a

s 1 e r et al. - Geologie ceske easti vnitrosudetske panve. (Eng. Sum.) Geology of the Bohemian part of the Intra-Sudetic basin. Dstr. U. Geol. Praha 1979.

STRESZCZENIE

Badania mikroflorystyczne karbonu polskich zagłębi węglowych (ryc. 1) mają długą historię, z tym że na ostatnie 30-lecie przypada ich intensywny rozwój. Dotyczy to szczególnie badań miosporowych prowadzonych w aspekcie stratygraficznym (2, 3, 6-10, 13, 14). Celem niniejszego opracowania jest zestawienie i podsumowanie wyników dotychczasowych badań, korelacja podziałów palinostraty-graficznych trzech polskich zagłębi karbońskich oraz parale-lizacja palinostratygraficzna pomiędzy zagłębiami polskimi i zagłębiami węglowymi Europy Zachodniej.

Podziały miosporowe karbonu poszczególnych zagłębi

węglowych Polski, przedstawione w niniejszym opracowa-niu, podsumowują głównie badania własne autorki,

do-tyczące Zagłębia Górnośląskiego i Lubelskiego. Dane dla

Dolnośląskiego Zagłębia Węglowego zostały zaczerpnięte

z publikacji innych autorów.

Na obszarze GZW w ostatnim IO-leciu wykonano wiele głębokich otworów wiertniczych, w ramach rozpozna-nia głębokich poziomów karbonu produktywnego.

Szcze-gółowe badania palinologiczne profilów tych otworów

dostarczyły obfitego materiału, który wyzyskano do

ze-stawienia podziału palinostratygraficznego pełnego profilu karbonu w tym zagłębiu - od facji węglanowej (górny turnej-dolny wizen(?)) po utwory stefanu. Wydzielono w tym profilu 14 poziomów sporowych, w tym 2 dla dinantu i 12 poziomów dla silezu (ryc. 2).

W Dolnośląskim Zagłębiu Węglowym stopień

roz-poznania palinologicznego utworów karbonu jest jeszcze

niepełny. Dokumentacja palinologiczna dotyczy głównie

formacji wałbrzyskiej, warstw z Białego Kamienia oraz

bezwęglowych utworów najmłodszego karbonu (górny westfal - stefan). Cennym uzupełnieniem jest opracowanie palinostratygrafii westfalu i stefanu czeskiej części zagłębia

(17). Zestawiając wyniki badań miosporowych w DZW z dostępnych publikacji wyselekcjonowano taksony miospor

ważnych stratygraficznie dla karbonu dolnośląskiego i po

uporządkowaniu i umiejscowieniu w profilu litostraty-graficznym zagłębia wydzielono 10 poziomów sporowych dla utworów silezu, w profilu od namuru A do stefanu

włącznie (ryc. 3).

Badania palinologiczne karbonu Lubelskiego Zagłębia

Węglowego; prowadzone bardzo intensywnie w ostatnim

dwudziestoleciu, dały podstawę do wprowadzenia

po-działu palinostratygraficznego karbonu w profilu od

gór-nego wizenu po westfal D. W profilu tym wydzielono 13 poziomów sporowych w tym jeden dla dinantu i 12 pozio-mów dla silezu (ryc. 4).

Porównanie zasięgów stratygraficznych taksonów prze-wodnich i charakterystycznych dla lokalnych podziałów

palinostratygraficznych pozwoliło wyselekcjonować te

tak-258

sony, które uznać można za diagnostyczne dla syntetycz-nego podziału miosporowego, wspólnego dla wszystkich trzech zagłębi węglowych (ryc. 5). Podział ten obejmuje utwory od górnego turneju -dolnego wizenu ( ?) do stefanu

włącznie. Wydzielono w nim 14 poziomów miosporowych oraz podano ich charakterystykę sporową, określono wiek poszczególnych poziomów i umiejscowiono je w profilach litologicznych poszczególnych zagłębi.

Syntetyczny profil palinostratygraficzny karbonu pols-kich zagłębi węglowych porównano ze zunifikowanym

podziałem miosporowym karbonu zagłębi węglowych Euro-py Zachodniej, zaproponowanym przez CIMP (1) (ryc. 6). Porównanie to wykazuje dużą zbieżność kryteriów

po-działu miosporowego i w większości przypadków

identycz-ność lub duże podobieństwo wydzielonych zon sporowych.

Różnice w występowaniu i zasięgach niektórych taksonów przewodnich wynikają prawdopodobnie z różnic w roz-woju facjalnym utworów tego samego wieku, które

spowo-dowały zróżnicowanie warunków ekologicznych dla roz-woju flory karbońskiej.

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