Bbl3BaHHblM ya~e scero MHOntMlll CTpaT111rpacp111YeCKlllMlll nepepb1BaM111 s ceA111MeHTau111111. BTopb1e 06pa3osan111cb s cpa3e sepT111KanbHoro npo6111saH111J1 coneM yepe3 Bb1wene->Ka~111e nopoAbl, Yero pe3ynbTaToM sisnsit0TCJ1 pacnpocTpa-HeHHb1e yrnoBble Hecornac111si Ili TeKTOHlllYeCKl!le KOHTaKTbl. 06a T111na consiHblX aHT111Kn111HaneM MoryT 6b1Tb npo-.nonrosaTb1e 111n111 6onee 11130MeTp111YecK111e; ycnosHoM
rpa-H111ue~ Me>KAY ~TlllMlll noArpynnaMlll sisnsieTCJI OTHOWeH111e AnlllHbl K w111p111He pas1-10 3:1. KoHTYP aHT111Kn111HaneM He npo6111sat0~111xcsi Yepe3 scKpb1wy - onpeAeneHHblM nyTeM aHan1113a MO~HOCTlll conJIHOM cep111111 HaXOAJl~eMCJI Me>KAY nOA- Ili HaACOnJIHblM ceMCMlllYeCKlllM rop11130HTOM - onpe-AensieT 1113onax111Ta 800 M. npoAOnrosaTble,. He npo6111sa-IO~llleCJ1 aHT111Kn111Han111 Ha3b1sat0Tcsi conJIHblMlll sanaM111, 6onee 11130MeTp111YecK111e - consiHblMlll noAywKaM111 (p111c. 1 111 2). AHT111Kn111Han111 npo6111sat0~111ecsi - cooTseTCTBeHHO: consiHblMlll rpe6HSIMlll 111 consiHblMlll CTon6aM111 (p111c. 3 111 4). HeconJ1Hb1e aHT111Kn111Han111 pa3AeneHbl Ha Tp111 noA-rpynnb1 B 3as111ClllMOCTlll OT 1113MeHeHlllM cpopMbl B
sepT111Kanb-HOM pa3pe3e, Bbl3BaHHblX 1113MeHeH111S1Mlll MO~HOCTlll. Bb1C0Ta Kp111nTOMOpcp111YeCKlllX aHTlllKnlllHaneM (p111c. 5- 7) yMeHbWlll-saeTCJI K sepxy 1113-3a yMeHbWeHlllJI MO~HOCTlll B COYneHeH-HblX napTlllJIX - OHlll MoryT 6b1Tb Aa>Ke COBCeM CKpblTble nOA MnaAWlllMlll CnOJIMlll. 3Tlll aHTlllKn111Han111 MoryT lllMeTb xapaKTep o6naYalO~lllX 111n111 KOMnaKUlllOHHblX CKnaAOK, HO OHlll Morn111 TaK>Ke o6pa3oBaTbCJI B CTaAllllll lllHBepc111111 . Hao6opoT, Bb1C0Ta cpaHepoMopcp111yecK111x aHT111Kn111HaneM
(p111c. 8-10) yMeHbWlllBaeTCJI K Hlll3Y - OHlll o6pa3osan111Cb
B MeCTe CTpYKTYPHblX ycTynos 111n111 snaAlllH c nepBlllYHO ysen111YeHHOM MO~HOCTblO ocaAKOB. Bb1C0Ta 11130Mopcp111-YeCK111x aHTlllKnlllHaneM (p111c. 11) OCTaeTCJI He1113MeHHOM Ha pa3HblX rop1113oHTax 111x pa3pe3a. Ase nocneAHllle n0Arpynnb1 06pa3osan111cb TOnbKO scne,aCTBl!le lllHBepClllBHblX ABlll>KeHlllM. BblABlllHYTblM cpopMaM cooTseTCTBYIOT noH111>KeHHb1e cpopMbl: Kp111nT0Mopcp111YeCK111e ClllHKn111Han111 c rny6111HOM ysen111Y111Ba10~eMCJI K Hlll3Y Ili cpaHepoMopcp111YeCKV1e ClllHKn111-Han111 c rny6111HOM yMeHbWlllBalO~eMCJI K Hlll3y.
SYLWESTER MAREK Geological Institute
THE QUESTION OF THE JURASSIC-CRETACEOUS BOUNDARY
IN MARGINAL ZONE
OF THE EAST-EUROPEAN
PLATFORM
UKD 551. 762.33/. 763.12.022 :565.33 + 563.12: 552.53/.54: 551.312/.313.1+551.35: 551.242.5(4-11)(438 -924.31 Niż Polski) The Teisseyre-Tornquist tectonic zone (TTZ)
repre-sents a sharp boundary of strongly uplifted basement of craton of the East-European Platform and an area of downwarped basement of the Paleozoic Platform of western and central Europe. TTZ and uplifted Variscan foldbelt situated further to SW separate a paleogeographic de-pression characterized by marked inherited posthumous lability and responsible for origin of Danish-Polish furrow along the former. This depression was the si te of sedimenta-tion of the thickest sequences from the Zechstein till the Cretaceous, inclusively. The whole Kujawy region was situated within the part of the depression with the highest rate of subsidence and affected by both transgressions coming from SE, i.e. Tethyan Ocean, and marine influences from already opened Atlantic.
Wide, lagoonal Purbeck reservoirs brackish in character and similar to those from the German and Paris basins, originated in the Polish Lowlands at the turn of the Jurassic and Cretaceous. The reservoirs became the si te of sedimenta-tion of carbonate-detrital-marly and lumachelle rocks, reflec-ting their freshening, as well as sulfate ones. The strata are underlain by the Middle V olgian with Virgatites pusillus (Michalski) (10) and overlain by marine Riasanian with
Riasanites rjasanensis (Wenetzky) Lahusen (22). Com-parisons with Anglo-German basins suggest that the Purbeck facies began to predominate in Kujawy part of the basin (Figure) in times of sedimentation of passage beds between lower and middle parts of the Miinder Formation, i. e. at the turn of the Portlandian and Purbeck sensu anglico (Table; see also 1, 6, 30).
The boundary between the Beriasella (Beriasella) jacobi and Beriasella (Pseudosubplanites) grandis zones, recom-mended as the Jurassic-Cretaceous boundary at the Lyon 1963 (1965) and Lyon-Neuchatel 1973 (1975) meetings (19), passes within the strata developed in the Purbeck facies (18).
248
In the Jura Mts, some limnic-lagoonal intercalations with ostracods have been found in lower parts of the Ber-riasian, characterized by the record of ammonites Beriasella
lorioli (Zittel), Beriasella richteri Oppel and Beriasella
privasensis Pictet. This made possible generał correlation of the Tithonian-Berriasian strata of SE France and time equivalents from the remaining limnic-lagoon basins of Europe.'
On the basis of ostracods it is assumed that the strato-type Jurassic-Cretaceous boundary coincides with that from upper part of the Lower Purbeck in England and between middle and upper parts of the Miinder Formation in the GDR and FRG (35, 16).
In the Kujawy region, central Poland, 6 ostracod zones have been differentiated in the Purbeck (from „F" to „A" -2, 24, 1).
Carbonate rocks of the zone „F", within which the Middle-Upper Volgian boundary has been delineated (10), yield brachiopods as well as euryhaline ostracods
Mantell-iana purbeckensis (Forbes) and first oligohaline ones of the genera Klieana and Rhinocypris.
Lower part of the zone „E" displays complete extinction of foraminifers. In the Kujawy region (central part of the sedimentary furrow), this zone is characterized by sulfate rocks with intercalations of limestones and marls with ostracods Fabanella ansata (Jones), Mantelliana
pur-beckensis (Forbes) and Klieana alata Martin. This ostracod assemblage is characteristic of the lowermost Purbeck in southern England and middle part of the Miinder Forma-tion.
The zones „F" and „E" correspond to the uppermost part of the Middle Volgian and lowermost Upper Volgian
(1 O), whereas „D", „C'' and „B" - presumably represent equivalents of the Upper Volgian.
The zone „D" reflects continuing predominance of the sulfate-carbonate facies. The recorded ostracods
in-2 T-T 3
--
o'""4..,._,..,,_..1-f#><fH...,'\
10 15 20 25 km
Marine basin in the Riasanian.
1
1 1 "\. "\. l l 1 /'..,.. (A.., 1 I l Ioriginal extent of sediments, 2 - directions of transgression, 3 - SW margin of the East-European Platform - the Teisseyre
--Tornquist tectonic zone.
Basen morski w riazaniu.
- pierwotny zasięg osadów, 2 kierunki transgersji, 3
-SW krawędź platformy wschodnioeuropejskiej - strefa
tekto-niczna Teisseyre'a-Tornquista.
BIOSTRATYGRAFIA POGRANICZA
TETYDA PROWINCJA
clude Cypridea dunkeri Jones and Cypridea aff. granulosa (Sowerby) in Oertli, characteristic of upper part of the Lower Purbeck in England and lower member of upper
part of the Miinder Formation - Katzberg Member
(30, 6).
The overlaying brackish-freshwater zones „C'' and
„B" are represented by marls and marły shales with
inter-calations of Cyrena lumachelles. The recorded ostracod
assemblage comprises the species Cypridea binodosa Martin,
C. cf. alta Wolburg and C. aff. propunctata
Sylwester--Bradley and Klieana kujaviana Bielecka et Sztejn, which make possible correlation of the two zones with lower part of the Middle Purbeck in England and German ser-pulite (2, 1).
The uppermost ostracod zone „A", confined to central parts of the Kujawy furrow, is brackish-marine in character
and developed as marły mudstones and sandy limestones
with Cyrena lumachelles. Besides Cypridea posticalis Jones, here were recorded marine ostracods Pachycytheridae compact a (Wolburg) and agglutinate foraminif ers Am-mobaculites kcyniensis Sztejn, Ammobaculites cf. eocreta-ceous Bartenstein et Brand. This zone reflects onset of Riasanian marine transgression in the Polish Lowlands and the strata gradually pass into marine ones with Ria-sanites rjasanensis (Wenetzky) Lahusen. The zone is cor-relable with upper part of the German serpulite and Mid--Purbeck Cinder layer which reflects Early Cretaceous marine ingression in southern England basin (4).
To sum up, the ostracod zones „D", „C", „B" and „A"
correspond to upper part of Lower and Middle Purbeck in England and the Katzberg and Serpulite members, upper parts of the Miinder Formation. The latter are re-garded as a member transitional between that formation and the Biickenberg Formation of the Weald (11, 16, 25, 26). Palynological data (19, 21) generally give support to the above outlined stratigraphic position of strata of the
Purbeck facies. This time interval was characterized by
marked predominance of plants of the family
Cheirolapi-JURY KREDY
BOR EA LNA TETYDA
SE Francja NE Anglia ~ Anglia RFN i NRD Niż Polski (Kujawy) Platfonro wscrodrioes~ka N Syberia, lk-al s Europa
Kw1 pertransiens Kw1 Paratollia Kw1 Tolypetf!11S Kw1 Neocomites + Kw1
Pseudogornierio Neotilo pertransiens Kw 1 mol'COUSlonum PloMenticeros ~oto-plicotilis klirrovskensis
j
>-Peregrinoceras al bi dum ~ ~ Suri tes
en §-g,
tzikwinianus - Bojar kia
ca llisto "' Surites miesezhnikowi
c Surites l Bojarkia) stenomphalus .D
;- spasskensis
"' .><
~ ·:,:-EliiliYmiceras,- -boissieri Surites ( Lynnia) icenii :::>
]
Euthymiceras Surites analogus boissieri>-- CD ·;;; Suntes
c: c --- ~ ---
----p1 c te t i o
~ Euthymiceras,
Hectoroceras o Riasanites Hectoroceras
~ 3 ł .g. Extemiceras,
param1mo - ko chi >--o "' ~ Hectoroceras koc hi occitanica
:g
Malbosicerasunum a::: c ~
kochi
~c A "'
dalm a si Runctonia runctoni CyprideoplSlicalis g Garniericeras Chetaites
Ammobotulites 0 subdypeiforme sibiricus grandis
--
. ~TL-- <%:11
Subcraspedites Serpuli I Klieona
occitanica
privasensis ( Volgodiscus) ~ o Kujowiana Chetaites
lamplughi >-
---c---
chetaeCypridea Graspedites
en c binadosa en >- nodiger ja cob i Subcraspedites = > f - - -:::t ,_ ___ 6_ ---- Craspedites
co subalpina
preplicomphalus :::;: -o Cypridea off. taimyrensis
gronuloso,
Cras~dites
Subcraspedites Katzberg C.dunkeri
grandis O" O" "" sutlditus c6i~neJ~les
( Swinertonia ) Kachpurites
primitivus
o,..._ ---E fulaens transitorius o
jacobi
>-"' P°oJ,~~~~~edites E >- Fa bonelio ansa to >- Epivirgatites E~rii~%m~1es nikitini
~ ~
>-"O
~ 3 ~ Mantełiono ~
3: ~ "'
.r.:
Fabanella oo ~ transitorius o.. Tita ni te s o o o Jllrbeci<ensis 3:
giganteus .>< ansata
o LL.. -o
>--o '-' c " ' o Virgotites Tajmyrosphinctes
o c
I - en :::'. Crendonites
~2 Virgotites ~ virgatus excentricus
o gore i
ce
V'I pusillus
daceae whereas the shares of conifers of the families Taxo-·
diaceae - Taxaceae -Cupressaceae were subordinate, and
those of the families Pinnaceae - Podocarpaceae - even
-somewhat lower. The share of ferns Filicales of the family
Gleicheniaceae appears negligible. The data indicate dry
and fairly warm climatic conditions. -·
Marine Riasanian sedimerits, occurring in sedimentary continuity with those of the zone „A", are assigned to the
beds with Riasanites and Malbosiceras. They are represented
by sandy mudstones, sandstones and sandy limestones
with fauna: Riasanites rjasanensis (Wenetzky) Lahusen,
Riasanites sp. sp., Praetolia cf. maynci Spath, Subcraspedites ( Pronjaites) sp„ Malbosiceras cf. malbosi (Pictet), Re-towskiceras cf. andrussovi (Retowski), Beriasella ( Picte-ticeras) cf. picteii (Jacob), Beriasella (P.) aff. picteti (Jacob) and Beriasella (P.) cf. jauberti (Mazenot).
In the Polish Lowlands, the overlaying strata of upper
marine Riasanian - beds with Euthymiceras and Surites
-are generally represented by claystones and mudstones
with Surites cf. spasskensis (Nikitin), Surites cf.
subtzi-kwinianus (Bogoslowski), Surites sp„ Externiceras sp„
Subcraspedites ( Borealites) sp„ Riasanites sp. div., Neo-cosmoceras cf. sayni (Simionescu), Neocosmoceras cf. fla-belliforme (Hegerat)," Ne6cosmoceras; cf. platycost~tum
(Sayn), Euthymiceras cf. euthymi (Pictet) and Beriasella
( Fauriella) sp. (cf. boissieri Pictet), Beriasella~sp. div. The Riasanian stra-:ta also yield bivalves, mainly of the
species Exogyra ·sinuata (Sowerby), and foraminifer and
ostracod rpicrofauna (33, 34). The foramiąifer assemblages
mainly comprise representatives of specieŚ with calcareous
tests: Lenticulina, Eoguttulina, Vaginulinopsis, Reinholdella,
Trocholina, Citharina and Epistomina, whereas of those
with agglutinated tests are less commó?n: M arssonella,
Lagenammina, Verneuilinoides, Trochamminoides„ Hap!o-phragmoides, Trochammina and Reophax. Ostracods are
here represented by the genera Protocythere, Schuleridea
and Cytherella. ·""?
Microfloristic studies ( 19, 20, 21) showed sudden extinction of plants Cheirolepidaceae and vivid development of conifers of the families Taxo_9.iaceae Taxaceae -Cupressaceae and Pinnaceae - Podocarpaceae at the
boun-dary of strata developed in the Purbeck facies and mari.ne
Riasanian. These phenomena were accompanied by marked
development of Filicales plants, especially those of the family Gleicheniaceae, whereas the share of horsetails Equisetales and club-moss Lycopodiales was subordinate. The vegetation indicates marked increase in humidity of
climate in relation to the Late Volgian (Purbeck).
The marine Riasanian of the Polish Lowlands appears well correlable with the Upper Riasanian of the Russian
Platform (22, 32, 28, 29, 31). Recent studies on lower
members of the Riasanites rjasanensis zone in arę.as of the
Pechora River and Oka River 'in the Moscow B~sin have
shown presence of two species of the genus Garniericeras
and Hectoroceras kochi Spath, highly important form
the point \of view of stratigraphy. Correlation of the Oka
River sections and those from the Mangyshlak region indicates that lower members of the Riasanian stage
cor-respond to the grandis zone (31). In the marine Riasanian
of the Kujawy furrow, equivalents of the lowermost mem bers
of the Riasanian stage with the fauna od Garniericeras
subdypeiforme, Hectoroceras kochi Spath and Riasanites
sp. div. are lacking. In Poland, the members are at least
parły replaced by strata of Purbeck brackish-!llarine
ostra-cod zone „A".
Correlation of marine Riasanian sections of the Polish Lowlands and those of the southern province shows that
250
the former mainly correspond to the Fauriella boissieri zone
(17, 18, 14).
The above analysis made it possible to draw the
follo-wjng stratigraphic conclusions:
- I ower ostracod zones „F" and „E", developed
in ·the Purbeck facies, represent passage beds of the Middle
and Upper Volgian;
- upper ostracod zones „D", „C" and „B"
pre-sumably represent equivalents of the Upper Volgian;
- the uppermost ostracod zone „A" represents initial
part of transgression of the Riasanian sea;
- the marine Riasanian comprises beds with Riasanites
and M albosiceras as well as Euthymiceras and Surites
(25, 26, 23, 27).
The recorded ammonites, mainly belonging to species
of the southern genera such as Fauriella, Malbosiceras,
Euthymiceras, Neocosmoceras, Picteticeras, Beriasella and
Retowskiceras, and those known from the Central Russia,
Riasanites, indicate that the initial transgression of the
Riasanian sea carne to Poland from south-east, i. e. western
Tethys. Ammonites of the genera Subcraspedites,
Ex-terniceras and Praetolina indicate influences from north--west, i. e . .from the northern Atlantic via the North Sea (22, 3, 7). A direct connection across East-German area presumably did not exist at that time as Wealdian strata known from north-eastern Mecklenburgia do not display
marine influences (12).
In the Boreal-Subboreal province, it is widely accepted that the Jurassic-Cretaceous boundary passes between
the Volgian and Riasanian, i. e. between the Subcraspedites
( Volgodiscus) lamp fug hi and Runctonia runctoni zones
in England, Chetaites chetae and Chetaites sibiricus zones
in Siberia, and Craspedites nodiger and Riasanites rjasanensis
zones in Russian part of the East-European Platform. A large part of Soviet researchers think that the Volgian--Riasanian boundary roughly corresponds to the strato-type boundary of the Tithonian and Beriassian, delineated
between the Jacobi and grandis zones (31, 15). According
to other researchers, the Volgian-Riasanian boundary
corresponds to a boundary · within the Beriasian in the
Tethyan province, passing at the base of the boissieri
zone (36, 32), within the occitanica zone or at the base of
the latter ( 15).
The above outlined differences in interpretations reflect remarkable difficulties in establishment of the Jurassic--Cretaceous boundary which could be treated as valid
for both the Tethyan and Boreal provinces. An
unequi-vocal determination of stratigraphic position of the Ria-sanian stage in the East-European Platform, where there are recorded ammonites of both southern and northern pro-vinces, may be of decisive importance for solving these questions. In the Polish Lowlands, any accurate definition of stratigraphic position of the Riasanian is impeded by the development of its lower members and, the Upper
Volgian in the Purbeck facies.
The analysis of results of stratigraphic studies on the Jurassic-Cretaceous passage beds implicates that
trans-gression of the Riasanian sea in the Kujawy furrow began
before the onset of sedimentation of strata of tl;ie boissieri
zone, in the occitanica zone. Strata of the marine-brackish
ostracod zone „A" originated at that time and marine
conditions began to predominate finally in the boissieri
zone. -?
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•
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32. S as o n o v a I. G., S as o n o v N. T. -· The Ber-riasian of the European realm. Zitteliana 10. 2 Sym-posium Kreide. Miinchen 1983.
33. Szt ej n J. - Foraminifera assemblages in the Valanginian of the Polish Lowland. Rocz. Pol. Tow. Geol. 1969 z. 2-3.
34. _Szt ej n J. - Mikrofauna kredy dolnej. [In:] Budowa
, geologiczna Polski. Atlas skamieniałości przewodnich i charakterystycznych. Cz. 3. Mezozoik. Kreda. Insty-tut Geologiczny. Wyd. Geol. 1984 (w druku).
35. Wie n ho 1 z E. - Zur Jura-Kreide Grenze in
der Deut~chen Demokratischen Republik. Erdol
-Erdgas. Information 1965 no. 7.
36. Z e i s s A. - Zur Frage der A.quivalenz der Stufen Tithon (Berrias/Wolga) Portland in Eurasien und
Amerika. Ein Beitrag zur KHirung der weltweiten Korrelation der Jura - /Kreide - Grenzschichten im
STRESZCZENIE
Granica jura - kreda, odpowiadająca w prowincji te-tydzkiej granicy tyton - berias ustalonej w spągu poziomu grandis, przypada wewnątrz utworów facji purbeckiej w limniczna-lagunowych basenach Europy Zachodniej.
W bruździe kujawskiej Niżu Polskiego w utworach
facji purbeckiej wyróżniono 6 poziomów małżoraczko
wych.
Węglanowe utwory poziomu „F", w obrębie których
przebiega granica między wołgiem środkowym i górnym,
zawierają obok ramienionogów euryhalinowe małżoracz
ki z rodzajów Mantelliana purbeckensis (Forbes) i pierwsze oligohalinowe małżoraczki z rodzajów Klieana i Rhino-cypris.
W poziomie „E", w którego dolnej części wygasają
otwornice, występują utwory siarczanowe z wkładkami
wapieni i margli z gatunkami Fabanella ansata (Jones),
Mantelliana purbeckensis (Forbes) i Klieana alata Martin. Poziomy małżoraczkowe „F" i „E" odpowiadają
naj-wyższej części wołgu środkowego i najniższej wołgu
gór-nego.
Poziomy małżoraczkowe „D", „C" i „B" mają cha-rakter brakiczno-słodkowodny i są zapewne odpowiedni-kami wiekowymi wołgu górnego. Najwyższy poziom małżo
raczkowy „A" ma już charakter brakiczno-morski. W poziomie tym występują, obok Cypridea posticalis Jones, morskie małżoraczki Pachycytheridea compacta (Wolburg) oraz zlepieńcowate otwornice Ammobaculites kcyniensis
Sztejn, A. cf. eocretaceous Bartenstein et Brand. Poziom
małżoraczkowy „A „ znamion uje początek transgresji
mo-rza riazańskiego.
Riazań morski reprezentują . warstwy z Riasanites i
Malbosiceras oraz Surites i Euthymiceras, korelujące się
w zasadzie z poziomem boissieri. Można wnioskować, że pierwsze ingresje morza riazańskiego nastąpiły przed poziomem boissieri w poziomie occitanica. Niestety
pro-fil riazania Niżu Polskiego, reprezentowanego w dolnej
części przez utwory facji purbeckiej, nie pozwala na
jedno-znaczne określenie jego pozycji stratygraficznej i ścisłą
korelację z innymi profilami prowincji borealnej i
tetydz-kiej.
marinen Bereich. Zitteliana 10, 2 Symposium Kreide. Mi.inchen 1983.
PE3IOME
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STANISŁAW KUBICKI, WACŁAW RYKA
Instytut Geologiczny
PÓŹNOPREKAMBRYJSKI
MAGMATYZM PLATFORMOWY
I
KARBONATYTY
W POLSKIEJ
CZĘŚCIPLATFORMY WSCHODNIOEUROPEJSKIEJ
UKD 551.22: 551.242.5]: 551.72: 552.33.08 + 552.4.08 karbonatyty: 553.07: 551.242.5(4-11)(438 -924.31 Niż Polski)
Krystalinik brzeżnej części platformy wschodnioeuro-pejskiej na obszarze Polski podatny był na dyferencjację
tektoniczną wyrażoną rozwojem dyslokacji nieciągłych,
rozczłonowaniem na wyniesione i obniżone bloki, a
także wielokrotnymi przejawami magmatyzmu
intruzyj-nego i ekstruzyjintruzyj-nego. Po konsolidacji gotyjskie.i
dezinte-252
gracja zachodziła z różnym natężeniem w jotniku, w
schyłkowym prekambrze, paleozoiku dolnym i górnym.
Z późnoprekambryjską aktywizacją
tektoniczna-mag-mową podłoża krystalicznego związane są intruzje
platfor-mowe, głównie typu centralnego. Należą do nich: alkaliczna--ultrazasadowa intruzja Tajna, alkaliczna-gabrowa
