deformacji typu fałdowego. W strefie okalającej strukturę AenJleMOH KaK cyAeTCKo-caCKO-TYP"1HrCKaJl 30Ha, "1ni.t W"1- sudecką tworzyły się w tym czasie osady asocjacji flisz~ pe - KaK cppaHKo-YewcKaJl 30Ha. 0Tno>KeHi.tJl MopaacKo wej a na pograniczu obu stref utwory typu olistostromów, -clorne3cKoiir 30Hbl npi.tHaAne>KaT K BHewHeH uen1-1 eapo zachowane dziś fragmentarycznie w strukturze kaczawskiej nei:1cK1-1x Bap"1CU"1AOB . i bardzkiej. - Kap6oH a npeAenax paccMaTp1-1aaeMoro pai'loHa npeA Utwory węglonośne wchodzące w skład zapadliska CTaaneH OCaAKaMi.t, aynKaHi.tTaMi.t "' "1HTPY3"1JlM"1 rpaHi.tT0- Sudetów Środkowych okteślono jako molasę młodszą, "1AOB. Pa3HOCTb B03pacTa, cpau1-1anbHoro npeACTaaneHi.tJl która zdeponowana została w wewnętrznej strefie łuku 1-1 CTeneHi.t npeo6.pa>KeH"1Jl oTno>KeH"1H coceAYK>Llli.tX c co- waryscydów europejskich. W tabeli przedstawiono k~ 6oi:1 B cyAeTCKOH CTpYKType, yKa3blBałOT Ha 6onbwoe relację jednostek litostratygraficznych silezu czeskiej i pol ropi.t30HTanbHOe nepeMell.leHi.te. npo"1CXOAJlll.1"1e OAHOBpe skiej części zapadliska Sudetów Środkowych. Molasa MeHHO aepT1-1KanbHb1e AB"1>KeH"1Jl Bbl3Ban"1 o6pa3oBaHi.te węglonośna Górnośląskiego Zagłębia Węglowego zloka B B"13ei'lcKoM 1!pyce B ueHTpanbHblX CyAeTax Me>Krop lizowana jest w strefie zewnętrznej łuku waryscyjskiego Horo nporn6a 3anonHeHHOrO OCaAKaMi.t Ti.tna MonaCCbl, a środkowoczeskie zagłębia węglowe leżą w obrębie wa He HapyweHHblMl-1 CKnaAl.faTOCTbłO. B 30He OKpy>1
ANTONI M. ŻELICHOWSKI Geological Institute, Rakowiecka 4, 00-975 Warsaw
THE CARBONIFEROUS IN WESTERN POMERANIA
UKD 551-735.1/.2.022 : 561/562 : 552.5(438-16 Pomorze Zachodnie) In the last two decades, Carboniferous strata have R . Dadlez (1) proposed subdivision of the Lower Car been encountered in some tens drillings in western Pome boniferous into a few complexes. In the --faiier subdIVłsfoil,' rania. Both the Dinantian and Silesian have been recorded quartz sandstones encountered beneath the Permian in there. The bistory of studies on these rocks goes back to over a dozen boreholes were assigned to the Upper Carbo 1961 when J. Poborski and L. Cimaszewski· described niferous, in accordance with contemporaneous strati Lower Carboniferous dolomites and daystones from the graphic interpretations. borehole column Bobolice 1. The progress in drillings Stratigraphic studies on Carboniferous and Devonian· works, mainly carried out by the oil industry as well as strata, initiated at the beginning of the seventies, questioned the Geological Institute, gave new boreholes of the Car.:. severa} earlier views (7, 21). H. Matyja (12) and K . Ko boniferous. The studies on macrofauna, carried out by rejwo (8-10) showed Tournaisian age of several sequences K . Korejwo (7), showed the presence of the Tournaisian, hitherto regarded as the Visean. Palynological analyses Visean and Upper Carboniferous. Drillings made in carried out by E. Turnau ( 19 - 20) showed that a part - area between Kołobrzeg and Chojnice revealed the presence of rocks previously assigned to the Upper Carbóniferous of Carboniferous · rocks markedly differing in lithology actually represent the Dinantian whilst H. Krawczyńska from those known in northern G.D.R. (6, 17) whilst the -Grocholska (11) and H. Kmiecik evidenced the presence Silesian resetnbling coeval strata from Riigen and northern of the Westphalian. The stratigraphic works were accom Mecklenburgia were found in area between Trzebiatów panied by petrographic analyses (4, 13), supplementing and Kamień Pomorski not before the mid-seventies. lithostratigraphy (1, 21 ). The lithology of Diriantian strata The stratigraphic studies were accompanied by attempts is here discussed with reference to lithological subdivision to establish local lithostratigraphic subdivisions made proposed by R. Dadlez and subsequently modified by the by J. Kuchciński, B. Sikorski, J. Ryba and A. Łobza, present author (22) and the Silesian - with reference mainly on the basis of well logs. Taking into account to the subdivision proposed by the present author. lithological differentiation of strata in the interval between In western Pomerania, Carboniferous strata have been Upper Devonian carbonate compl ex and Permian rocks, found in a bełt stretching along the Baltic coast from the
356 CORRELATIONS OF THE CARBONIFEROUS IN NORTHERN GDR, NORTHERN POLAND AND LATVIA
Northern GDR Northern Poland - Pomerania Latyia Northern Riigen Is. NW part Central part**, NE part Mecklemburgia and Hiddensee Is. Kamień Pomorski, Świdwin, (17) Koszalin, i (~_._?) '. Trzebiatów Bydgoszcz Brda
1 .,.._. Monchguter Sch. i::~ 160m ·a.§ ~ _...... _ ---- ,...... _ ...... / ~ ~ I -...... ~ "'-./" ~ '-./" 'v' Dziwna Formation Dziwna Fm. 68+170 m t5fr< 1 R amb" mer Sc h . - , 95 +248 m 150+170 m , ·
Trenter Sch. 100 _+130 m o brown-red siltstones Dornbusch Sch. Rega Fm. - 180_+200 m 130_+170m ~
u t------....1 s
1 t<--- with ~" • .., • „ i... i.. Jasmunder Sch. sandstones and """ ~ ~ '.~ 270+310 m conglomerates at the sandstones, ~ ..c:: Wolin Fm base 180-330 m siltstones, coals, ~ -+------1-ł 41_+282 m .(825 m) marine horizons I.I„"" ... """""""'"'"' .... ""' ...... "" ·107_+404 m ~ Lohmer Sch. 25_+50 m „ ~i.------4-1 ~,,~J ~~ ... ~~~ ... ~~~~~ ... ~ < Wieker Sch. 50 + 70 m ,-„„ Hiddenseer Sch. 40 _+ 50 m J" i..""'"""' -: itfflh a~d 5Jalkow _s~~ ~- „ ' - -• .~;::s i:i:i cla'y"ollo~ ~ ~~ stones, stigmana ~ .: 1~-~~:'"rriri~ ,„ . - ,J . ' ,.. ,_. ", 1.o ...... ,. ... ,i.,. ... „i,.."'-...... ,.--.....~.... ~-ui....., "'""'~i..,,,..i..„ claystones, Riigenls. - Nadarzyce Complex Hiddensee sandstones, mar Is, over 250 m >"' sandstones, conglomerates limestones claystones 400_+500 m over over 300 m - 400m >"' Drzewiany d Q Kurowo Complex Complex oj ~"~ oj up to 400 m ~ "'.... ~ 400 m a gb oj > a > limestones a a oo~ o ,,,a I oo __Kurow9 Complex 500 m ~i)':~ dO >~ I o >.- or- over 150 m .; t1 ~ +. ~+ 8 uO >.o ;.:: .Q ~ ~~
- a a "'oo dO "'oo i::"' • o!"'"\ do E-< :at:.; + • O N i::"' ~~ + E-< Chmielno ; ~g ; ~o Łobżonka Complex Supercomplex d Eo- a-os„. d -~ -~ over 300 m up to 400 m * "Nic - Ńicaskaja ISui te,: Lie - Lietiżhskaj~ j S11ite ~ ! Pap - Paplakskaja I Sui te. ** Strata here assigned to the Silesian are regarded as the Rotliegendes in (14, 15). 357 vicinities of Kamień Pomorski to Koszalin and also from grains, debris of trachytes, rhyolites and volcanic glass the latter town to Chojnice. South-west of the Koszalin - as well as quartz grains and micas. Among feldspars, Chojnice zone, single drillings entered the Carboniferous, K-feldspars varying in degree of alteration, kaolinitiza failing to reach its base. tion, carbonatization and sulfatization predominate. Some feldspars display regeneration rims. No direct sources LITHOLOG I CAL-ST RATIG RAP HIC of volcanic materiał were found in Pomerania and Dinan CHARACTERISTICS tian volcanism is here represented by diabase dykes only (4). Dinantian Sandstones occurring in eastern and western parts of this region are mainly built ·of quartz (Trzebiechów In western Pomerania, the Dinantian is subdivided complex). Some anhydrites from the Kołobrzeg area ori into a .few lithological complexes, i.e. informal units which ginated in result of epigenetic changes of feldspars and when formalized will correspond to the lithostratigraphic others - in result of evaporation. ones of the formation rank. The supercomplex differentiated The Chmielno supercomplex is 400 m thick, wedging here corresponds to group. out to NE. Using the available stratigraphic data (8, 10, The Sąpolno complex is regarded as the lowermost 12, 20), it is dated at the Tournaisian and Visean. Datings lithostratigraphic unit of the Dinantian. It is recognized obtained for the SW -NE section show that sedimenta in borehole columns in area between Trzebiatów, Kosza tion of its rocks started in the Early Tournaisian (Tnl b-2), lin and Brda, and it comprises an interval characterized being delayed until the Visean in NE and SW parts of by presence of clay-siltstone and sometimes .calcareous this region. rocks. lt ha~ bee!! found in both sections displaying con The Drzewiany complex rests on ,rocks of the Chmielno tinuity at the Devonian-Carboniferous boundary and supercomplex or, locally, directly on the Lower Paleozoic. those with gaps at that boundary. The Sąpolno complex It comprises ·rock packet 400 m thick, mainly composes is varying in thickness. Limestone and marły intercala of wackes and quartz arenites with intercalations of clay tions in claystones are built of biomicrites with admixture stones, limestones and dolomites. Some stigmaria horizons of pelloids and quartz dust. Brachiopod microfacies pre were also found. Palynological (20) and ostracod data dominates in biomicrites, being accompanied by crinoidal, make possible ·assignation of these rocks to the Upper bivalve, ostracod, foraminifer, bryozoan and algal-serpulid Tournaisian and Visean. Distribution of the rocks is limited microfacies. to NE part of the ~rea. The available stratigraphic data (8, 10, 12, 20) show, The Nadarzyce complex also · rests on rocks of the that rocks of the Sąpolno complex belong to Tnl b-2 or Chmielno supercomplex but in areas situated further to Tn3. They are usually underlain by those of the Człuchów SW. It comprises an almost 250 m packet of claystones, complex of the Upper Devonian. Top parts of the latter calcareous in lower part. The roćks were dated at the are dated at the Famennian or the lowermost Tournaisian Upper Visean. (Tnla). The Chmielno supercomplex, resting on rocks of the The Lobżonka complex has been found in central and south-eastern parts of area of distribution of the Dinan Sąpolno complex, represents a clear-cut lithostratigraphic unit in the Dinantian of Pomerania. A specific lithological tian. lt comprises clay-siltstone rocks with intercalations composition gives it fairly autonomous character. lt is of quartz, sometimes calcareous wackes. There were also characterized by presence of sandstones of the arcosic found numerous tuffite horizons. The rocks are overlain wacke type, party lithic, and oncolitic-oolitic limestones, by oo lite limestones of the Kurów complex or rock younger accompanied by siltstone and clay rocks, sometimes with than the Carboniferous. Their base was still not penetrated anhydrite intercalations. Marked lithofacies differentia by drillings but the thickness may be estimated at several tion of the Chmielno supercomplex · makes possible its hundred meters. The rocks were assigned to lower Visean subdivision into lower-rank units. Intervals with pre and Tournaisian. dominance of oolitic limestones, sometimes epigenetically The available dąta on lithology of the Dinantian in changed, are called the Kurów complex after R. Dadlez Pomerania and the stratigraphic ones indicate that its (1) and clay-siltstone packets with anhydrite intercala sedimentation was differentiated and varying in time. tions - the Grzybów complex. The Gozd complex (for The above described Dinantian section of Pomerania merly Wierchowo coniplex - 1) is proposed for the essentially differs from that of the Lublin region, intervals comprising arcosic and lithic wackes and the characterized by paralic Upper Visean strata resting Trzebiechów complex - for sections with small share directly on pre-Carboniferous strata, although both Po of ooids and presence of wackes and quartz arenites (see meranian and Lublin basins were situated at the margin Fig. 2). of the same East-European Precambrian Platform. In the Chmielno supercomplex, limestones form layers varying in thickness. They are usually built of ooids with Silesia n admixtures of oncolites, peletoids, intraclasts and bioclasts as well as ortochemical components such as micrite and Rocks assigned to the Silesian discordantly overlay sparite and quartz, feldspars and sulfates. Some quartz the Dinantian and often older ones. Rocks undoubtedly and feldspar grains belong to allochemical components. belonging to the Upper Carboniferous are known from Limestones of the Kurów complex represent the oolitic the Trzebiatów - Kamień Pomorski and Sarbinowo - Ko facies proper whilst those of the TrŻebiechów complex, szalin areas. Whereas rocks of the red beds association, yielding both ooids and extraclasts ( quartz, feldspars . occurring in the Świdwin - Bydgoszcz area are treated and volcanic materiał), - the mixed oolitic lithofacies. as the Upper Silesian or, which is more widely accepted, The oolitic limestones sometimes display stromatolites. Lower Permian. Because of differences in lithological Arcosic, sometimes lithic wackes predominate among development between the three areas, they are separately sandstones of the Gozd complex. They are built of feldspar discussed below. 358 ...... oo o ~ ' CHOJNICE @ ""-. o 0o ··.. •. SZCZECINEK o 0""-. ··········· ··. .. o o o "- - Cz.1 * ····· .... ······· • Cd * ~* Cs(n) * • ··. .. * • ···. • ?~ * * o 3 BYOGOSŻCZ ~ 0 PIŁ~ -_.;,..4 /. O 30km ?~ * . ..·· Ryc. 1. Szkic podpermskich wychodni karbonu. Fig. 1. Sketch map of Permian subcrops of the Carboniferous. Otwory wiertnicze, w których stwierdzono: 1 - karbon górny, Boreholes encountering: 1 - Upper Carboniferous, 2 - Lower 2 - karbon dolny (dinant), 3 - utwory starsze od karbonu, Carboniferous (Dinantian), 3 - rocks older than Carboniferous, 4 - wybrane uskoki, 5 - obszary występowania utworów czer 4 - selected faults, 5 - areas of occurrence of Rotliegendes rocks wonego spągowca, zaliczane przez autora do wyższego silezu, regarded as Upper Silesian by the present author, 6 - boundaries 6 - granica obszaru podlegającego denudacji w trakcie turneju, of area subjected to denudation in Tournaisian, 7 - boundaries 7 - granica obszaru podlegającego denudacji w niższym turneju, of area subjected to denudation in Early Tournaisian; Bab - Bab - Babilon 1, Bob - Bobolice 1, Br - Brda, Chm - · borehole Babilon 1, Bob - Bobolice I, Br - Brda, Chm - Chmielno, Cz 1 - Czaplinek IG-1, Drz - Drzewiany 1, Go - Chmielno, Cz 1 - Czaplinek IG-1, Drz - Drzewiany 1, Go - Gozd, Grz - Grzybowo, Ko - Koszalin IG-1, Ku - Kurowo, Gozd, Grz - Grzybowo, Ko - Koszalin IG-1, Ku - Kurowo, Strz - Strzeżewo, Wie - Wierzchowo, D - dewon, Cd - dinant, Strz - Strzeżewo, Wie - Wierzchowo; D - Devonian, Cd - Cs(n) - namur, Cs(w.,-s) - westfal i stefan, Cs(w) - westfal. Dinantian, Cs( n) - Namurian, Cs( w - s) - Westphalian and Ste- phanian, Cs(w) - Westphalian. THE TRZEBIATÓW - KAMIEŃ POMORSKI AREA · generally indicative of the Silesian. Palynological analyses In this area, strata assigned to the Silesian are up to of samples from middle part of the section (H. Kmiecik, 700 m thick but individual sections are markedly varying unpubl. report) showed their Westphalian C age: mixed in the preserved thickness due to advanced epigenetic assemblages with Florinit'es sp. sp„ Vestispora fenestraia erosión. They rest either on the Dinantian or Devonian (Kosanke et Brok.) and V. costata Balwie (Bhardawaj). and, similarly as in Riigen Id. (16), are overlain by intrusive On the basis of correlations with Riigen sections (2, 5, rocks of Rotliegendes conglomerates built of pebbles 18),-the Wolin formation is dated at the Westphalian A - of the latter. Three formations are differentiated in the lower Westphalian C and treated as ań equvalent of the section of Silesian strata here (from the base upwards): beds from Hiddensee, Wiek, Lohme and Jasmund. Wolin, Rega and Dziwna formations. The Rega formation comprises a higher part of the The Wolin formation comprises lower part of the sec section, 130- 170 m thick arid characterized by an in tion and its recorded thickness is varying from 44 to 282 m. creased share of sandstones and presence of innumerous. I t is characterized by cyclic sedimentation. Six cyclothems conglomerate horizons. Sandstone layers are varying in . 30 - 70 m thick were recognized in. the most complete thickness (up to 30 m at the most) whereas siltstone-clay o( the studied sections - Strzeżewo section. The number intercalations are generally thin. The latter sometimes and thickness of cyclothems decrease toward~ north-east, display appendices and stigmaria and aerial portions where finally only the top cyclothems are found. of plants: e.g. horsetail stems, leaves of ferns such as The Wolin formation begins with 20 m packet of sand Pecopteris polymorpha. Rocks of the Rega formation are stones. Higher cyclothems are built of siltstone-clay rocks mottled, red-brown to cherry-brown in colour, with grey and sandstones whilst the lower alsa display limestones. or green spots, except for sandstones which are sometimes Colour of rocks changes from grey and dark-grey in lower light-grey. The latter are represented by fine- to medium part of the section to mottled, mainly brownish in the -grained quartz arenites and wackes, resembling those upper part. Plant remains are here represented by both of the underlying formation in petrographic composition. aerial and subaerial (stigmaria) portions of plants. More Quartz (sometimes with regeneration rims) is the major over, thin laminae of coals were found here. rock-forming component and the share of debris of silice Sandstones of the Wolin formation belong to quartz ous rocks and feldspars (sometimes corroded) is here wackes and arenites· with small admixture of feldspars subordinate. Matrix is varying from clay and ferruginous and debris of siliceous rocks and micas. In their matrix, to siliceous, calcite (presumably rełated to alteration of illite and kaolinite are accompanied by carbonates, sulfates feldspars) and sulfatic. and, in a higher part of the section, marked admixture The paleontological record is here limited to the above of ferruginous matter. cited Pecopteris polymorpha as palynological analyses Aerial portions of plants found in the above strata - showed the presence of innumerous Lycospora sp. and (Paripteris/Neuropteris) gigantea (Sternberg) - are Sporonites sp. and Acritarcha assemblage without bio- 359 Czaplinek IG 1 b 0 j-:_-12 ? (w ES:js ~8 y 11 16 5045,5-'. j 1 012 * u ~ !:-: .:- .„ ~3 [2:]6 c:==J9 -·-·-17 >- r. 13 N ~4 [g10 Q> 14 .. · 18 o \ ~7 "'O T 15 19 o z * \ Karsina 1 Drzewiany1 Pz Brda 1 -"' Wierzchowo 9,i 2476,0 llJ \ ·.·.-.·:~os.o Q. p E Cle \ - I ~ !...... (...!... C) \ ~§ o ~7·%"""-. . ~~ ...,.,, . \ E .... a;c: . co t1' "' ~Cl E o .c 3: ~ ""'·" N u :: ;:J ~ -"' llJ Q. ~ E ~ o -"' "'O o o -"' c: -"' llJ a. -"' E c: o -o -"' •N ..o o ...i -"' llJ o. E ~ ·...:.j:....= T óOOó.O Ryc. 2. Zestawienie wybranych profilów otworów wiertniczych Fig. 2. Comparistfń of selected borehole columns of the Dinantian. z osadami dinantu. l - columns: a - cored interval&, b - lithology, 2 - claystones 1 - profile: a - miejsca pobrania rdzeni, b - litologia, 2 - and siltstones, 3 - marły limestones, 4 - limestones, 5 - dolo iłowce i mułowce, 3 - wapienie margliste, 4 - wapienie, 5 - mites, 6 - anhydrites, 7 - calciferous rocks, 8 - presence of dolomity, 6 - anhydryty, 7 - wapnistość osadu, 8 - dolomi dolomite, 9 - quartz sandstones, 10 - arcosic and lithic sand tyczność osadu, 9 - piaskowce kwarcowe, 10 - piaskowce arko stones, 11 - record of microflora, 12 - microfauna, 13 - macro zowe i lityczne, 11 - stwierdzona mikroflora, 12 - mikrofauna, fauna, 14 - ooids, 15 - tuffites, 16 - red colour of rocks. Bound 13 - makrofauna, 14 - oolity, 15 - tufity, 16 - czerwona bar daries of lithostratigraphic units: 17 - between complexes, 18 - wa osadu. Granice jednostek litostratygraficznych: 17 - między within Chmielno supercomplex, 19 - stage boundaries. Mio kompleksami, 18 - w obrębie nadkompleksu z Chmielna, 19 - spore assemblages differentiated after E. Turnau (20): Ma - granice pięter. Wydzielone . zespoły miosporowe na podstawie Dictyotriletes major, Cl - Prolycospora claytoni (a, b, c - pracy E. Turnau (20): Ma - Dictyotriletes major, Cl - Prolyco- subzones). spora claytoni (a, b, c - podzony). stratigraphic value. Taking into account sedimentary con tion of these rocks to the uppermost Westphalian and tinuity with underlying formation and analogy with Stephanian. However, it is 1not excluded that the upper reference to the Riigen sections, the formation is inter most strata belong to the Autunian. The Dziwna forma preted as of the Upper Westphalian (higher Westphalian C tion is correlated with upper part of the Trent and' Rambine and D?). Upper boundary seems to be diachroneous. and Monchgut Beds. The strata are correlated with the Dornbusch Beds and presumably a part of the Trent Beds. THE KOSZALIN AREA The Dziwna formation comprises the uppermost part In the vicinities of Koszalin, a packet of sandy rocks of the Silesian in the vicinities of Trzebiatów and J<_a with claystone intercalations with coally hands, assigned mień Pomorski. lt is up to 240 m thick and built of complex to the Silesian, have been found beneath the Permian in of brown-red siltstone rocks with marked share of sand two boreholes only. The strata are up to 400 m thick. stones and conglomerate horizons. Sandstones are represented by quartz wackes and arenites Sandstones of that formation belong to ,quartż wackes with content of rock debris and feldspars usually below and arenites and, in part, lithic wackes. Quartz, often with 1 %. Cement is formed of clay mass as well as ferruginous authigenic rims, is the major component here but rock matter and sulfates. The clay intercalations yield horizons debris occurs in somewhat larger amounts than in lower with linguloid fauna and pectens: Lingula mytiloides formations. Besides fragments of siliceous rocks, here Sowerby, L. elliptica Phillips, Pterinopecten cf. speciosus occurs debris of intrusive on.es. Kaolinitized and sometimes Jackson as well as Anthraconia cf. prolifera var. valida sericitized and carbonatized feldspars are fairly rare. Waterlot and Schisodus antiqua Hind. Spore analyses (3) Matrix appears similar as in underlying formations. showed the presence of redeposited Dinantian specimens · N o organie remains were found here, except for frag and those indicative of the Westphalian, including Flo ments of Annularia sp. and Calamites sp. reported by rinites mediapudens. This made possible assignation of K. Korejwo. Microphytoplankton is here innumerous the strata to the Westphalian. They may represent an whereas both pollen and spores are missing. The correla equivalent of the Wolin F ormation in the Trzebiatów - tions with the Riigen sections (5, 18) made possible assigna- Kamień Pomorski area. 360 Strzefewo 1 Czaplinek IG 1 Ryc. 3. Profile silezu z części nadmorski(j obszaru Strzeżewo ( stre P1 fa Trzebiatów - Kamień Pomorski) i Koszalin (strefa Koszalina). 3199,0 4588,5 o o o <'-· Objaśnienia jak na ryc. 2, ponadto: 1 - występowanie flory, 2 - obecność stygmarii, 3 - obecność ,węgli, 4 - pstra barwa osadu >.. o o o * ::i c: • O ·o· (1 - miejsce stwierdzenia zespołu sporowego z Florites spp. 31: ::i * oraz Vestispora fenestrata i Schopfipollenites sp. (H. Kmiecik), N c o 2 - miejsce stwierdzenia przez K. Korejwo raripteris ( Neuro ...: * pteris) gigantea, 3 - miejsce stwierdzenia przez T. Migierową 3442,5 Paripteris polymorpha. * O> Fig. 3. Silesian sections in coastal part of .the Strzeżewo (Trze Q) y QJ * a:: ~@ Koszalin IG 1 biatów - Kamień Pomorski zone) and Koszalin (Koszalin zone) ...: * areas. 3608,0 y,...,2339,0 .... y* l - record of flora, 2 - presence of stigmaria, 3 - presence of c y 5045,5 c c: * Cv3 coals, 4 - mottled colour of rocks; 1 - record of spore assemblage * with Florites spp. and Vestispora fenestrata and Schopfipollenites ~ -- y r-. t Ryc. 4. ł sp. (H. Kmiecik), 2 - records of Paripteris (Neuropteris) gigantea QJ ·~ ...... Fig. 4. by K. Korejwo, 3 -'-- records of Paripteris polymorpha by T. Mi- :;: o gierowa; other explanations as given in Fig. 2. . ~ „ ·--- • .e QJ 3890,0 Ryc. 4. Profil osadów „czerwonego spągowca", w którym stwier 03 :;: występowanie zespołów y r-. ~ dzono sporawych silezu z Thymospora sp...... Ryc. 3 . 2763,0 ~i ?6' 1 ...... 2 -3 *4 Cv Fig. 3. Fig. 4. Sections of "Rotliegendes" rocks found to yield Silesian spore assemblage with Thymospora sp. tion is impossible. Macrofloral remains are also innumer .THE ŚWIDWIN - BYDGOSZCZ (CENTRAL) AREA ous and of limited stratigraphic value so the stratigraphic data based on results on microfaunistic and palynological Spore assemblages found in strata of the Drawsko analyses (8, l O, 20, 22) are most numerous. Of the micro formation (grey siltstones and sandstones) in central fossils, most important are here conodonts which made and south-western Pomerania show that this formation, possible delineation of the Devonian-Carboniferous boun assigned to the Rotliegendes (14-15) may comprise some dary and identification of the Tournaisian (12). Identifica Upper Carboniferous rocks. Taking this into account I tions of foraminifers in thin ~ections made possible dating supposed (22) that sedimentation of the red beds associa limestones of the Kurów complex which often do not tion started in the Late Silesian (Westphalian) to continue yield any macrofaunal remains. The 'results of palynological in Permian. In result of formation of a wedge of red rocks, analyses (3, 11, 19 - 20) also appeared highly important marine ingressions coming from w·estern Europe to south here. -eastern Poland became cut off in the Late Carboniferous. The differences in biostratigraphic methods used in This seens to be shown by the youngest marine horizons studies on the Carboniferous of Pomerania, accurate in the Lublin region, dated at the tum of the Westphalian correlations are no.t always possible and the subdivision A and B ( equivalents of the Katarzyna horizon). Silesian accepted in the stratigraphic table often represents the rocks of Pomerania, interpreted as above, will also com results of attempts to average the data. prise intrusive rock covers. Upper Carboniferous volcanism Low er bo u n dary of the Carbonifero us was accepted were not known from marginal part of the East-European in accordance with resolutions of the n Congress on Platform until the last years. Recent drillings made in Carboniferous Stratigraphy, i.e. at the base of the Gatten area between Warsaw and Toruń revealed an intense dorfża stage. ,Thus some intervals of the sections, represent volcanic event which preceded sedimentation of the West ing equivalents of the lowermost Tournaisiati (Tnla) phalian. It has been responsible for origin of trachytes and assigned to the Carboniferous by K. Korejwo (8, and rhyolites and pyroclastic materiał is present thrciughout 1O), are excluded from that system here. the Westphalian section. I do not treat the question of The presence of the Tournaisian is evidenced is several Silesian age of a part of rock packets hirtherto assigned sections on the basis of spore assemblages, conodonts to the Lower Permian as solved but ratller a hypothesis and ostracods. A gap in sedimentation, corresponding for further studies. to lower Tournaisian (Tnl b-2), has been found in the Koszalin area. At that time, strata of the Sąpolno complex SYNT.HETIC SECTION and, in part, Chmielno supetcomplex' were originating OF THE CARBONIFEROUS in areas further to the south. In the Late Tournaisian (Tn3), the Chmielno supercomplex • aną. some parts of the Drze The above discussed lithostratigraphic units comprise . wiany complex were formed in the north, and at least the whole section of the Carboniferous. The results of a part of the Łobżonka complex in central Pomerania. stratigraphic studies, given in discussions on individual The sedimentation of strata of the Drzewiany complex lithostratigraphic units, clearly show diachroneous nature was contłnuing in the Visean in the north whereas in the of the latter. It should be also noted that the stratigraphic south the Visean is represented by top parts of the Łob subdivision is based on plant and faunal remains varying żonka complex, Kurów complex and the top of the Na in value so the units cannot be treated as of the same rank. darzyce complex. Macrofauna is rather innumerous, being mainly represented Strata assignable to the Namurian are still not known by bivalves and brachiopods. Goniatitids are occiasional in this region and the oldest Upper Carboniferous strata here and usually so poorly preserved that specific identifica- recognized here on the basis of palynological ~ata are of 361 the Westphalian age. The Westphalian here comprises Analysis of Dinantian sections of Pomerania shows the strata from the Kamień Pomorski area (W o lin, Rega that we are dealing there with normal regressional sequence, and, partly, Dziwna formations) and Koszalin as well' connected with transition from neritic to littoral facies. as red clastic rocks from the Szubin - Bydgoszcz zone. The oolite limestone facies of the Kurów complex, prevail The Stephanian age assumed for a part of the Dziwna ing in the north in the Early Tournaisian, was gradually formation and red clastic rocks in central Pomerania is migrating to develop in central part of the studied region still not based on biostratigraphic data. at the tum of the Middle and Late Visean. The sedimenta The above discussed section of the Carboniferous tion of the Dinantian ended with sandy rocks of the Drze in Pomerania is clearly bipartite. Its lower part, belong wiany complex, representing a sandy wedge migrating ing to the Dinantian, comprises strata ranging in age towards the south at the top of the section. In the north, from the Tournaisian to Upper Visean, and the upper these rocks form the whole section of the Dinantian, and (Silesian) - strata assigned to the Westphalian and Ste in the south - the top part onl~. It is not excluded that phanian. They are separated by a stratigraphic gap corres further to the south such sediments were originating in ponding to the Namurian. The gap is traceable in area the Namurian, w hen a large part of Pomerania was emerged NE of the Kamień Pomorski - Bydgoszcz line. and subjected to denudation. The above discussed Dinantian rocks are markedly SOME REMARKS varying in original thickness (of over 300 m). They range ON SEDlMENTARY ENVIRONMENT in paleothickness from about 300 - 400 m in the north · AND BASIN MORPHOLOGY to over 1200 m in central Pomerania. Paleoisopachs are oriented oblique in relation to the controlled tectonic In Pomerania, Carboniferous strata are represented lines, close to W - E. by platform formations formed in relatively mobile area. Vertical movements of individual blocks were markedly The area was characterized by increased rate of subsidence differentiated in intensity in the Namurian, when large and sedimentation, except for some erosional events. part of the region was subjected to denudation. Amplitudes It was situated in far foreland of the Variscan geosyncline, of the movements, calculated on the basis of extent of entering the area of the East-European Precambrian Plat ero si on of Dinantian rocks, range fr om 1OO - 200 m to form. 1 over 1,000 m. · Sedimentary basin of the Diflantian represented a con The Erzgebirgian phase in the Variscan geosyncline tinuation of the Late Devonian one. An infraformational has been followed by downwarping of the foreland and gap is traceable in northern part of the studied area and a beginning of a new sedimentary cycle in Pomerania. uplifts of individual blocks resulted in local angular un The cycle began with sedimentation of coal-bearing associa conformities. Upper Devonian strata are already regressiye tion replaced in the Late Westphalian by that of red clastic in character. Similarly as the. Dinantian, they are terrigen rocks. The onset of sedimentation of the latter was, howe ous in the north or· carbonates clearly displyiang traces ver, contemporaneous with ·the appearance of coal-bear of advanced shallowing. The movements were accompanied ing strata in some parts of Pomerania. This was due to by volcanic phenomena, the results of which include pyro origin of the wedge of red rocks, responsible for cutting clastic materiał in rocks of the Chmielno supercomplex off connections between the Lublin Basin and Carbonifer or diabase dykes or sills ( ?) cutting the rocks. ous sea of western Europe. A new stage in volcanic activity, The above discussed rock complexes clearly show typical of the Early Permian, began in the Late Silesian. shallow-water character of sedimentation. The analysis of facies distribution in the Dinantian showed that strata LITERATURA occurring in the north have originated close to coastal 1. D a d 1 e z R. - Podpermskie kompleksy skalne w line. It should be noted here that the present NE boundary strefie Koszalin-Chojnice. Kwart. Geol. 1978, nr 2. of distribution of Dinantian strata is related to pre-Zechstein 2. D 6 ring H. - Sporstratigraphische Untersuchun epigenetic erosion. In the coastal area, where the boundary gen im Bereich des Silez ("Graue Folge") aus dem coincides with a fault zone, the section clearly displays Raum Nordhiddensee. Z. Geol.' Wiss. 1975, H. 3, gaps and increase in content of sand at the Devonian nr 7. -Carboniferous boundary whereas the sections of De 3. Górecka T., Park a Z. - Stratygrafia osadów vonian-Carboniferous passage beds are continuous and karbonu - otworu wiertniczego Koszalin IG-1 na developed in clay-marly facies further to SE (e.g. Brda podstawie badań palinologicznych. Pr. Nauk. Inst. area). As it was noted by E. Turnau (20), we are often Górn. Pol. Wr. 1980 nr 35, Studia i Materiały 1980 dealing with a hiatus or advanced condensation. Iled nr 16. clays, common in the Tournaisian in northem part of the 4. He f 1 i k W., Muszyński M. - Diabazy z wier region well reflect the course of denudation processes in cenia Kurowo 2 koło Koszalina. Kwart. Geol. 1973 neighbouring land areas. Red continental strata are also nr 3. known from the Devonian-Carboniferous boundary in 5. Hi r s c hm a n n G., Hot h K., K 1 e ber F. - the borehole columns- in western Lithuania and Latvia. Die lithostratigraphische Gliederung des oberkarbons The differentiated movements of basement blocks im Bereich der Inseln Riigen und Hiddensee. Z. Geol. resulted in differences in character of sedimentation in Wiss. 1975 Bd: 3, H. 7. individual parts of the basin. Rocks of the Gozd complex 6. H o ff m a n N., L i n d e r t W., et all. - Zum have originated in offshore shoals whereas those of the Unterkarbon - Vorkomen auf den Insel Riigen und oolitic facies proper of the Kurów complex appear related Hiddensee. Ibidem. ' to shoals situated further from the coast. Debris of igne 7. Kor ej w o K. - Stratigraphy and paleogeography ous rocks and ooids were transported by bottom currents of the Namurian in the Polish Lowlands. Acta Geol. to basins separating the above shoals in which clay-marly Pol. 1969, t. 19 nr 4. sedimentation was taking place. This resulted in origin 8. K o r ej w o K. - The Carboniferous of the Chojni of rocks of the mixed. oolite facies (Trzebiechów complex). ce area (Westem Pomerania). Ibidem 1976 t. 26 nr 4. 362 . 9. Kor ej w o K. - Charakterystyka litologiczna i roz zasadzie odpowiada randze formacji, a wydzielony nad wój paleotektoniczny karbonu w rejonie Wierzchowa kompleks - grupie. (Pomorze Zachodnie). Ibidem 1977 t. 27 nr 4. W obrębie osadów dinantu wydzielono następujące 1O. K o r ej w o K. - Biostratigraphy of the Carbonifer jednostki: kompleks z Sąpólna, nadkompleks z Chmielna, ous sediments from the Wierzchowo area (Western kompleksy z Drzewian, Nadarzyc i Łobżonki. Pomerania). Ibidem 1978 t. 28 nr 4. Kompleks z Sąpólna stanowi najniższą jednostkę lito 11. K r a w c z y ń s k a - G r o c h o 1 s k a H. - Z badań stratygraficzną, w całości należącą do dinantu. Reprezen palinologicznych karbonu północno-zachodniej Pol towany jest on przez pakiet skalny o zwiększonym zaile ski. Prz. Geol. 1975 nr I. niu osadów i zaniku sedymentacji węglanowej. Spoczywa 12. Maty j a H. - Biostratigraphy of the Devonian on na utworach kompleksu z Człuchowa (górnego fa -Carboniferous passage beds from some selected pro menu, a po części turneju) lub na starszych osadach. Jest files of NW Poland. Acta Geol. Pol. 1976 t. 26 nr 4. to jednostka diahroniczna rozwinięta w turneju (od dol 13. Muszyński M. - Charakterystyka mineralogicz nego do górnego). no-petrograficzna karbońskich skał osadowych niecki Nadkompleks z Chmielna, występujący na znacznym pomorskiej (okolice Bobolic). Pr. Miner. Kom. Nauk obszarze ponad osadami kompleksu z Sąpólna stanowi Minerał. PAN Oddz. Kraków 1976 t. 48. jednostkę samoistną. Odznacza się charakterystycznym 14. Pokorski J. - The Rotliegendes of the Polish składem litologicznym: liczne piaskowce i zlepieńce, typu Lowland. Prz. Geol. 1976 nr 6. wak arkozowych i litycznych, rzadziej kwarcowych, po 15. Pokorski J. - Propozycja formalnego podziału wszechne wapienie oolitowe, onkoidowe, a także obecność litostratygraficznego czerwonego spągowca na Niżu anhydrytu. Zmiany facjalne i następstwo facji pozwoliło Polskim. Kwart. Geol. 1981 nr I. na wydzielenie w jego obrębie mniejszych jednostek - 16. Ros t W., Sc hi ma n s k y W. - Ubersicht iiber kompleksów, których· nazewnictwo wzięto za R. Dadle das Oberkarbon und das Rotliegende im Nordteil zem (1), niekiedy je modyfikując. Kompleks z Kurowa der DDR. Ber. Deutsch. Ges. Geol. Wiss. A. Geol. stanowią w przewadze wapienie reprezentujące fację ooli PaHiont. 1967 Bd. 12 H. 3-4. tową właściwą. Tworzą je wapienie oolitowe i onkoidowe 17. Schmidt K., Fr a n k e · D. - Stand und Pro o grubości od kilkunastu do blisko 400 m. Obok peloidów, bleme der Karbonforschung in der Deutschen De intra- i bioklastów występuje także mikryt i sparyt oraz mokratischen Republik T. I - Unterkarbon. Z. Geol. kwarc, skalenie i siarczany. Kompleks z Gozdu zwany też Wiss. 1975 Jh. 3, H. 7. kompleksem z Wierzchowa ( 1) w większości tworzą waki · 18. Schmidt K., Fr a n k e D. - Zur lithologisch arkozowe, niekiedy lityczne piaskowce i zlepieńce. Obok faziellen Entwicklung des Prapermes im Nordteil der licznych skaleni spotykane są okruchy i ziarna trachitów, DDR. Z. Angew. Geol. 1976 nr 11. ryolitów, szkliwa wulkanicznego i kwarcu. Kompleks z Grzy 19. Tur n a u E. - Microflora of the Famennian and bowa utworzony jest ze skał mułowcowo-ilastych, zawiera Tournaisian deposits from boreholes of Northern jących przewarstwienia i soczewki anhydrytu. Natomiast Poland. Acta Geol. Pol. 1975 t. 25 nr 4. osady ilasto-mułowcowe z nielicznymi ooidami i prze 20. T u r n a u E. - Korelacja utworów górnego dewonu warstwieniami piaskowców typu wak kwarcowych wy i karbonu Pomorza Zachodniego w oparciu o badania dzielono jako kompleks z Trzebiechowa. Miąższość utwo · sporowe. Rocz. P. T. Geol. 1979 t. 49 nr 3-4. rów nadkompleksu z Chmielna osiąga 400 m. Wiek tych 21. Że 1 ich owski A.M. - Karbon [W:] Ropo- i ga utworów przypada na turnej (w części N) i ku południowi zonośność obszaru nadbałtyckiego między Świnoujś przechodzą one do wizenu. ciem a Darłowem na tle budowy geologicznej. Cz. I - Kompleks z Drzewian, są to w przewadze utwory pias Budowa geologiczna pod red. R. Dadleza. Pr. Geostr. kowców (do 400 m) o typie wak i arenitów kwarcowych, Inst Geol. 1971. spoczywające na osadach nadkompleksu z Chmielna lub 22. żel ich owski A.M. - Karbon [W:].Budowa geo bezpośrednio na starszym paleozoiku. Datowany jest on logiczna wału pomorskiego i jego podłoża, pod red. , na turnej i wizen. Kompleks ten rozwinięty jest w N części A. Raczyńskiej. Pr. Inst. Geol. (w druku). obszaru. Kompleks z Nadarzyc występuje w południowej części STRESZCZENIE Pomorza bezpośrednio nad wapieniami kompleksu z Ku rowa. Reprezentują go iłowce liczące ok. 250 m. Dato W wyniku prowadzonych prac wiertniczych, uzyskano wany jest on na wyższy wizen górny. w ciągu ostatnich 20 lat kilkadziesiąt profilów wiertniczych Kompleks z Lobżonki ma podobne rozprzestrzenienie osiągających utwory karbonu. Na ich podstawie stwier jak poprzednio wymieniony i złożony jest z mułowców dzono występowanie utworów dinantu i silezu. W wyniku i iłowców z przewarstwieniami wak kwarcowych. Spoty badań stratygraficznych (3, 7, 8, 9, 10, 11, 12, 19, 20 i 22) kane są w nim poziomy tufitowe. Podścielają one utwory udokumentowano obecność turneju, wizenu oraz west kompleksu z Kurowa lub wychodzą bezpośrednio pod falu. Osadów namuru, wbrew pierwotnym przypuszcze młodszymi osadami. Datowania wskazują na niższy wizen niom (7, 21), nie stwierdzono. Wydzielenia osadów ste i turnej. Zazębianie się tych kompleksów przedstawiono fanu dokonano w nawiązaniu do opracowań pochodzą na ryc. 2. cych ~ NRD. Badania petrograficzne (4, 13, 22) wskazują Osady silezu występują w trzech obszarach, wykazując na zróżnicowanie charakteru skał zarówno węglanowych, znaczne zróżnicowanie. W strefie Trzebiatów - Kamień jak i klastycznych. Pomorski (ryc. 1, 3), wśród osadów zaliczonych do silezu Silne zróżnicowanie litologiczne, a także trudności wydzielono trzy formacje, od dołu: Wolina, Regi i Dziwny. w badaniach biostratygraficznych skłoniły do wprowa Odznaczają się one zmiennymi proporcjami skał ilasto dzenia dla osadów karbonu Pomorza Zachodniego lokal -mułowcowych i piaszczysto-zlepieńcowych. W najwyż nych podziałów litostratygraficznych (1, 9, 22). Wydzie szej pojawiają się okruchy skał wulkanicznych (Dziwny). lane jednostki litostratygraficzne mają charakter jednostek Na podstawie badań palinologicznych udokumentowano, nieformalnych dla dinantu. Przyjęta nazwa kompleks w że wyższa część formacji Wolina należy do westfalu C. 363 Reprezentuje ona asocjację węglonośną, w stropie formacji 1.1eCKMX MCCne.o,oBaHMH np1111.1111cneHbl K Kap6oHy. 3.o,ecb Wolina mamy do czynienia z zamianą jej na asocjację . y.o,oKyMeHTMpoBaHO pacnpocTpaHeHMe OTno>KeHMH TypHeH skał czerwonych. Ślady roślin . struktur korzeniowych, CKoro, BM3eHcKoro 111 aecT MARCIN PIWOCKI Geological Institute, Rakowiecka 4, 00-975 Warsaw BROWN COALS IN POLAND; CHARACTERISTIC OF OCCURRENCES UKD 552.576.l :552.14+553.96.068.l :551.762/.78(438) The distribution of deposits and other occurrences brown coa1s are known to occur in the Lower and Upper brown coals in individual structural units in various parts Jurassic, Upper Cretaceous and Tertiary. Economic value of the country have been discussed by several authors of Mesozoic brown coals is nowadays rather limited. (e.g. 2, 3, 10, 16), mainly in papers dealing with more generał The major, currently mined brown coal deposits are stratigraphic, tectonic and deposit problems. In Poland, connected with the Mjocene (Figs. 1 - 2) but the coals 364