SUMMARY
The differentiation of Jurassie and Cretaceous litho-stratigraphic units in the Tatra Mts may be treated as an example of introduction of "The principles of Polish stratigraphic classification". This formanzation is here critically analysed with reference to principles of dif-ferentiation of lithostratigraphic units in the Alpides. The use of the Pieniny names in the Tatra Mts, especially in the case of units differing in development (as e.g. Pie-niny Limestone Formation or Krupianka Limestone For-mation) is treated with reservation. The differentiation of the Dunajec Group in the Tatra M ts appears unfounded. Similar is the case of assigning various lithological sequences spongiolites and crinoid and red limestones -in a s-ingle Buciska Limestone Formation as the sequences may be better treated as separate formations. Reserva-tion is also made with reference to justificaReserva-tion of formaliza-tion of the Choc Jurassie sequence in the Tatra Mts as the Miętusia Limestone Formation with several members. Better profiles of both the Choc Jurassie and Krizna Lower Cretaceous (differentiated as the Kościeliska Marł Formation) are known in Slovakia and stratotypes for these units should be selected in the latter area. M ore-over, the subdivision of the Raptawicka Turnia Lime-stone Formation should be supplemented by differentia-tion of members.
It is stated that principles of formalization should be established in cooperation with geologists from the neighbouring countries, especially Slovakia, in order to avoid multiplication of names by naming parts of units separated by state boundary. The formalization should be aimed at obtaining more precise definition of mapp-able lithostratigraphic units and not giving new names for not always sufficiently known sequences.
PE31-0ME
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M.O. UMENWEKE Anambra State University of Techno1ogy
SCARCITY OF MIOSPORES FROM ALBIAN SECTION AT FOLKESTONE, ENGLAND
The purpose of this paper is to record the miospore assemblage of an Albian section at Folkestone, Southern England and to account for their impoverished nature and similarity to Jurassie and Aptian roieroflora. The palynological study of the English Albian has attracted much interest because of the interesting and continuous record it presents of the rise of angiosperm pollen (see E.M. Kemp, 8) and because of its usefulness in stratigra-phic correlation especially in confirmation and refinement of ages of otherwise unfossiliferous nonmarine deposits. Apart from that the middle and upper Albian rocks of England are well-dated and have been thoroughly studied on basis of macrofossils and the desire to compare pałyno logical assemblages with other macro- and micropalaeon-tological assemblages such as ammonites, ostracods, and foraminifera was one of the initial objectives of the study. This was not possible again due to scarcity of spores and pollen.
One of the earliest studies of Mesozoic palynology in England and Scotland was made by R.A. Couper (3)
UKD 561 :581.33:551.763.13(420) who systematically described dispersed spores and póllen grains. G. Norris (11) published his descriptions of mio-spores assemblages from the Purbeck beds of Southern England and from the Upper Kimmeridgian and Portłand ian marine sediments exposed on the Dorset coast. He further examined the stratigraphic value of miospores for zonation and correlation of strata developed close to the Jurassie- Cretaceous boundary in Southern England. The study of Aptian and Albian miospores of Southern England was made by E.M. Kemp (8). She emphasized the appearance of angiosperm poJlen in Aptian and Albian and persistence of pre-Albian forms in the Gault Clay (Middle and Upper Albian).
Later J.F. Laing (lO) made a description of angiosperm poJlen from the Albian and Cenomanian strata of both Southern England and Northern France. He described twenty-two (22) species of angiosperm poJlen assemblages and rela.ted them to the ammonite zones of the Albian stage. The above-mentioned works are not exhaustive of the enormous literature available now but they are
important to the present paper for the authors studied the palynology of areas nearest or inclusive of the present study area as will be shown later. E.M. Kemp (8), J.F. Laing (10) and M. Umenweke (25) contain a lot of references on Albian palynology in Britain.
METHOD OF STUDY
The rock sampies used in the study were macerated using standard palynological techniques which principally involved dilute hydrochloric acid (HCl) which was used to remove the carbonate while 10% HF was used to dis-solve the silicates. Safranin O was used for staining. The sampies were stored in the Palynology Labaratory of the Department of Geology, King's College, University of London, where the work was done. The sample number, the slide, the minimum size, the number of specimens measured, and the maximum sizes are stated against the palynomorphs. Sampies were colected from each am-monite zone established for the section (see H.G. Owen, 16 and Fig. 2 of this study).
STRATIGRAPRY AND GEOGRAPHICAL LOCA TION OF SAMPLES
In England, the Lower Albian is represented within the top beds of the Lower Greensand and its junction with the overlying clays of the Gault. The Gault Clay is divided broadly into Lower. Gault and Upper Gault which correspond respectively with the Middle and Upper Albian substages as shown in Fig. 2.
The sampies were taken from each ammonite zone established by H.G. Owen (14, 16) of the Gault succession at Copt Point and East Wear Bay, Folkestone, Kent (Figs. l, 2). The section is regarded as one o f Albian standard sections since the work of F.G. Price (17). The elassie section is included by A.D. d'Orbigny (1840-42) in his list of standard ·localities when defining the Albian stage. The section is also described in some detail by de C.E. Rance (19) in W. Topley's Memoir (24).
The Gault at Folkestone consists of Beds I to XIII. The section at Copt Point consists of Beds I to XI while, adjacent to the Coastguards Lock out below the Martello no. I Tower in East Wear Bay, the upper parts of Beds
O IOmls ~
KEY o 10 20 km
~ Gault outcrop ~ Upper Greensand outcrop
Fig. l. Map of the Wea/d showing positions of Folkestone and Gau/t
outcrop
Ryc. l. Obszar badań
XII and XIII are exposed. Mobile landforms made sample collection from Beds XII and XIII rather · very difficult. The junction of the Lower Albian and the Gault Clay is defined by presence of Sulphur Bands at the base of the Gault and current-bedded clayey sandstones of the Lower Greensand. The clay is bluish, sticky and contains many courses of phosphatic nodules. The Upper Gault Clay is very calcareous and in many other localities passes into a diachrono_us sandy facies called Upper Greensand. The Albian and Cenomanian boundary is defined by the Glauconitic Marł of the Lower Cenomanian.
The description of the section is as follows:
Bed XIII: fawnish grey marły clay 8.84 m mottled light grey and fawn grey 0.91 m. Highly glauconitic light grey clay highly glauconitic at base but diminish upward in size and number 3.95 m;
Bed XII: highly glauconitic light grey clay with scattered phosphatic nodules and a seam of them at base 0.99 m; Bed XI: pale grey marly clay with phosphatic nodules bed at base 10.67 m;
Bed X: tough light grey marly clay with phosphatic nodules at the top and in a seam at 0.73 m below top 1.55 m;
Bed IX: light grey marly clay indurated at top which is marked by phosphatic nodules. Mar1stone lenticles occur between 0.76 and 1.70 m above base, 2.85 m;
Bed VIII: (in part) grey clay, phosphatic nodules 0.6m;
Bed VII: grey clay with pyritized fossils 2.6 m; Bed VI: mottled clay, grey and glauconitic nodules 0.32 m;
Bed V: glauconitic nodules, dark 0.5 m; Bed IV: grey clay, pyritic 0.16 m;
AGE BEO SINo AMMONITE ZONE 28
~l
f-27 z 1-26 c{-
1-2!5 ID l-..1 -24 S ta liczkola ..l ::::l o"'"'
1- dispar 1!1 -23 a:: -22 a:: LU ~ 0.. LU O.. -210..=
o -20 0.. LU Martoniceras ::l ID -19 1n f l a tu m -18 -17 E u hoplit e s -16 lautus z~l
-1!5 c{ -14 ID l-..1 -13 Euhoplites ..l ::::l -12 lori c atu s e~:"' 1!1 o -11 a:: 1-LI.ILIJ -10 ..l :t o~ - 9 ~ o...
- 8-
- 7 Hoplites ::E o dentatua LU ID - 6 -!5 - 4 a:: Z UJe{ - 3 OouvlcellacHas :t ;Q - 2 mommillotum o ..l ..Ie~: - lFig. 2. Generalized section showing Albian substages, samp/e points
and Ammonite zones
Ryc. 2. Zgeneralizowany pro.fil. z podziałem a/bu, miejscem
po-brania próbek i zonami amonitowymi
Bed III: grey clay 2 m; Bed II: grey clay 2.6 m;
Bed I: grey clay, sandy, base of the Gault 3.6 m.
RESULTS
As shown in Fig. 2, the Albian standard section at Folkestone is zoned on basis of ammonites as follows (14-16):
_ Stoliczkała dispar Zone Sample Nos 22-2~ Mortoniceras inflatum Zone Sample Nos 19-21 Euhoplites lautus Zone Sample Nos 16-18 Euhoplites loricatus Zone Sample Nos 11-15 Hoplites dentatus Zone Sample Nos 6-10
Douvicellaceras mammillatum Zone Sample Nos 1- S The Lower Albian is represented by D. mammi/latum Zone, the Middle Albian by H. dentatus, E. loricatus and E. lautus and the Upper Albian is represented by M. inflatum and S. dispar Zones.
As shown in Fig. 3, the five sampies taken from Lower Albian sediments yielded the foilowing species named below:
Podocarpidites radius, Araucariacites australis, Den-soisporites perinatus, Gleicheniidites senonicus, Comcavissi-misporites varirerrucatus, Alisporites elon~atus. C/asso-pollis torosus, Podocorpidtes minimus, Cengulitritetes sp.,
Microfoveolatosporites sp., Classopollis hamenii, gymno-sperm poilen and woody plant materiaL
The Middle Albian sediments (Samples No. 6 -18) on the other hand yielded many species of which the foilow-ing appear for the first time:
Cyathides australis, Matonisporites eqwexinus, Par-vissaccites radiatus, Cyathides punctatus, Microreticu/ati-sporites diatretus, Lycopodium austroc/avatidites, K!uki-sporites sp., C/assopollis c/assoides, Po/ypodiaceaesporites sp., Cf. Cicatricsisporites ha/lei, Lycopodiumsporżtes ex-pansus, Todisporites major, Appendicisporites potomacen-sis, Pinuspollerites sp., Cf. Rubinella major and pałyno logical materials like foraminiferal shell linings and spe-cimens of coccolith.
The Upper Albian on the other hand yielded most of the species already recorded for the Lower and Middle Albian but seem to be characterised by presence of tri-porate poilen and absence of the foilowing species: G/eiche-niidites senonicus, Alisporites e/ongatus and Pinuspolle-nites sp.
The state of preservation of the palynomorphs varied from one time- unit to the other. For instance the species in the Lower Albian were poorly preserved and some of them were mechanically damaged. In the Middle Albian, most of the species were very well preserved and were more abundant than those of the Lower Albian. The Upper Albian witnessed a decrease in specimen abundance of most of the species. Their preservation was good.
One of the most striking features of the palynomorphs was their state of preservation. Most of the palynomorphs were well preserved in the Gault Clay and morphological damage or deformation was rarely observed. Recycled or reworked spores arid pollen were easily identified by their very dark colour. The palynomorphs of the Lower Albian (upper part of Lower -Greensand) were not as well preserved as those of the Gault. Pyrite crystals were boldly emplaced on some specimens and quite a good number
L OWER MlDOLE A L 8 l A N U PP ER ALB lA N
A LISIA N (LOWER GAULTl (UPPER G AULTl
Ma m millatu m Dentotus Loricałus Lautus olnflatum Olspar
.!. N (11 • Ol Ol.." Cli q)
o
- - (;; ; o; - ~ iii .L N ~ N N N N - N Ol q) o N (11 -C> Ol X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X lf X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X XFig. 3. Distribulion of palynomorphs in the Albian of Southern England N N Cli .." X X X X X X X X X N CJI T A X A
CYATHIDITES AUSTRALIS Couper 19!!19
MATONISPORITES EQUIEXINUS CCouperl Dettman 1963
PODOCARPIOITES RADIU S Slngh 1971
PARIIISSACCITES RAOIATUS Couper 19e9 ARAUCARIACITES AUSTRALIS Cookson 1947
LYCOPOOIUMSPORITES AUSTROCLAIIATIOITES (Cooksonl Potonic 1~56 CYATHIDITES PUNCTATUS B renner 196.3
DENSOISPORITES PERINATUS Couper 1959
KLUKISPORITES SP.
GLEICHENIIDITES SENONIGUS Rouse 1949
MICRORETICULATISPORITES OIATRETUS Norris 1969
CONCAVISSIM l S POR l T ES VARIIIERRUCATUS CCouperl Brenner 1963
ALISPORITES ELONGATUS Kemp 1970
CLASSOPOLLIS GLASSOIDES Pocock and Sansoniu s 1~81 CLASSOPOLLIS TOROSUS (Rel .. ingerl Couper u~e9 CENGULITR ILE TES SP.
POLYPODIACEAESP.ORITES SP.
Cf. CICATRICOSISPORITES HALLEI Oelcourt and Sprumont ·~e& Cf. RUBINELLA MAJOR Couper 1958
POOOCARPIDITES MINIMUS Couper 1958
LYCOPODIUMSPORITES EXPANSUS Slngh 1971
TODISPORITES MAJOR Couper 1959
APPENDICISPORITES POTOMACENSIS Brenner 1963
MICROFOVEOLATOSPORITES SP.
CLASSOPOLLIS HAMENII Burger 1966
PINUSPOLLENITES SP. TRIPORA TE POLLEN GYMNOSP!RM POLLEN S HE L L: LININGS COCCOLITH PLANT MATERIAL
were mechanically damaged and corroded. The poor preservation of the palynomorphs of the top of the Lower Greensand was probably due to the sandy lac1es of the Lower Greensand. The good preservation afforded by the Gault Clay was expected due to the fact that it is a marine clay and offered a cushion effect on the specimens which prevented not only microbial attack but mechanical da-mage.
The greatest concentration of the number of specimens and species was in the Middle Albian (Lower Gault). Both the Upper Albian and Lower Albian showed eonsictera ble drop in the number of specimens of each species.
The area covered in the study is too narrow to warrant any generalization. The poor preservation of the Lower Albian (Lower Greensand) and the increased water depth in the Upper Albian (16) were perhaps contributory
fac-Fig. 4. All.fłgures magnifled x 250. The order ofrecording is: specfes name, size (minimum, number o( specimens, maximum), samp/e
number and slide in bracket plus microscope coordinates
- Cyathidites punctatus Brenner 1963 40 (15) 55 microns F10 (6) 113 -12.50; 2 - Matonisporites equiexinus (Couper) Dettman 1963 48 (11) 58 microns F9 (5) 112.7 -12.7; 3 - Klukisporites sp. 40 (30) 54 microns F3 (8) 94- 32.00; 4 - Lycopodiumsporites austroclavatidites (Cookson) Potonie 1956 38 (17) 45 microns F8 (l) 150-26.50; 5 - Araucariacites australis Cooksan 1947; 6, 9, 10, 11 - Parvissaccites radiatus Couper 1958 40 (28) 60 FlO (4) 113 -45.00; 7, 8 - Podocarpidites radiafus Singh 1971
overall size 60 (30) 70 microns FlO (2) 115-44.50
Ryc. 4. Wszystkie okazy są powiększone 250 x. W opisie podano:
nazwę gatunkową, wielkość (minimalną, liczbę okazów,
maksy-malną), numer próbkt i - w nawiasie - numer preparatu oraz
współrzędne mikroskopowe
tors to their scarcity. Even though shelf assemblages can easily be swept by contemporaneous marine currents into deeper water as remarked by D. Habib (6), the Middle Albian (Lower Gault) sea was pro ba bly nearer the land and vegetational source than the Upper Albian hence more palynomorphs occur in the latter.
Another striking feature of these Albian miospores
is its similarity with spores and pollen from the Cat lsland,
North Atlantic in Bahamas and Jurassie forros in Britain.
D. Ha bib (5) described some spores and pollen of Albian
age recovered from abyssał depth (5200 km) in submarine
outcrops near Seismic Ret1ector Horizon Beta in Cat
lsland, Bahamas. Most of the species described by E.M.
Kemp (8) and this study bear close resemblance or are
identical to those of D. Habib (5). Apart from confirming
the Albian age of the Gault, the following species are
common to both areas: Todisporites major, G/eichenitdites
Fig. 5. All.fłgures magnifles x 250. Explanations as given in Fig. 4
l - Densoisporites perinatus Couper 1958 48 (6) 60 microns F (l) 118-11.00; 2 - Cf. Rubinella major Couper 1958 (11) 50 microns F9 (3) 112- l 0.00; 3, 4 - Cicatricosisporites Cf. C.
hallei Delcourt and Sprumont 1955 40 (21) 55 microns F15 (5) 112-39.00; 5 - Microfoveolatosporites sp. F4 (6) 109-35.50; 6, 7, - Gleicheniidites senonicus Rouse 1949 40 (18) 50 microns F7 (2) 110-9.7; 30 (15) 40 microns F2 (3) 118- 38.00; 8 - C
lasso-pollis hammerinii Burger 1966 F6 (8) 113- 32.00; 9 - Triporale
pallen 20 (13) 30 microns F6 (8) 120- 21.00; 10 - Cingulitritetes 28 (11) 35 microns F7 (2) 122-44.00; 11 - Lycopodiumsporites
expansus Singh 197140 (13) 60 F8 11-32; 12-Cyathidites
australis Couper 1958 45 20) 60 microns Fl4 (l) 105-48.00
Ryc. 5. Wszystkie okazy są powiększone 250 x. O~jaśnienia jak dla ryc. 4
senonicus, Cicatricsiporites australiens1s, Parv1ssaccites ra-diatus, and Cyathidites australis.
In Britain, G. Norris (11) studied miospores from the Purbeck Beds and marine Upper Jurassie of Southern England. The species w h ich are observed in bot h the Jurassie and Albian are as follows: Araucariacites australis, Microreticu/atisporites diatretus, Parvissaccites radiatus, Ap-pendicisporites potomacensis, Gleicheniidites senonicus, C/as-sopo//is torosus, Concavissi miosporites variverrucatus and
Lycopodżumsporites expansus. Apart from these, many of the spores described by G. Norris were also recorded by E.M. Kemp (8) from various Aptian and Lower Albian sections in England. lt does appear that there was no marked difference between the flora of the Jurassie and the overlying the Lower Greensand and Gault. The most notable difference was the emergence of the angiosperm pollen in Aptian and their increase in Albian.
The impoverished nature of the assemblage in this study merits special mention. The Gault and its arenace-ous facies, the Upper Greensand, are relatively poor in
Fig. 6. All.fłgures magn(fłed x 250. Explanations as given in Fig. 4
l - Gymnosperm poilen F3 (4) 110-00; 2 - Alisporites elon-gatus Kemp 1970 60 (15) 80 microns F9 (6) 110-25.00;
3-Pinuspollenites sp. F (8) 120 11.00; 4 - Podocarpidites minimus
(Couper) 1958 40 (11) 50 microns F11 (4) 110- 33.00; 5 - MiCI·o-reticulatisporites diatretus Norris 1969 30 (8) 40 microns F9 (5) 11 O- 34.00; 6, 7 - Classopol/is classoides Pocock and J ansonius 1961 30 (12) 40 microns F6 (8) 102-34.00; 8, 9, 10 - Classopol/is torosus (Reissinger) Couper 1958 35 (11) 45 microns FI O (3)
109-38.00
Ryc. 6. Wszystkie okazy są powiększone 250 x. Obja.fnienia jak dla ryc. 4
plant megafossils although drifted wood is abundant (see 8, p. 134). J.M. Stopes (23) described a cone of prob-abie bennettitalean origin from an unspecified Gault Horizon at Folkestone. The scarcity of the spores and pollen could therefore probably be a reflection of the environment of deposition ratber than a reflection of the hulk composition of flora living in Gault times. The Lower Gault was deposited in about 150-200 m water depth (7) and the Upper Gault was much deeper (25). The presence of woody remains (see this study Fig. 7, specimens 2, 6) in the Lower Greensand (Lower Albian) and absence of fern foliage has been attributed to a large ex tent to the destruction of leaves and more delicate organs before burial and to the long period of transportation suffered by remains deposited under marine conditions (20, 8, 9, 23). lt can therefore be safely stated that the impoverished nature of spores and pollen in the section under study is related directly to the distance of the sea from land or vegetational source and environment of deposition. The angiosperm pollen which are more com-mon in the Gault and Lower Greensand are so smali in size (on the average below 35 microns) as observed by E.M. Kemp (8) and J.F. Laing (10) that they can be
trans-Fig. 7. A/l.figures magn(fied x 250. Explanations as given in Fig. 4 l - Shell Liningsofa trochoid foraminifera F10 (11) 109-27.00 Middle Albian; 2 - Plant material F11 (3) 117 -42.00; 3
-Coccolith sp. F13 (8) 110-13.00; 4 - Todisporites major Couper 1958 40 (11) 50 F8 (3) 110- 32.00; 5- Concavissimisporites variverrucatus (Couper) B renner 1963 45 (30) 65 F11 (7) 11 O- 36.00; 6 - Plant material F6 ( 4) 11 O- 28.00; 7 - Appendicisporites
potomacensis Brenner 1963 45 (20) 60 F7 (3) 110-108
Ryc. 7. Wszystkie okazy są powiększone 250 x . Objaśnienia jak dla ryc. 4
ported long distances in the open sea without much dif-ficulty.
On the French side of the Anglo-Paris Basin, J.C. Foucher and Ph. Taugourdeau (4) recorded only fourteen (14) undescribed and unnamed spores and poilen plus other microfossils from Albian section in Wissant in France. The forms they figured are trilete spores and conifer pollen. The scarcity of spores and poilen in the Albian sediments is therefore not just a local feature peculiar to Folkestone (England) but is true of the neigh-bouring French Albian section.
The study of some Albian section in Folkestone has shown that spores and poilen are impoverished and well preserved except in the top part of the Lower Greensand below the base of Gault. The spores and pollen composi-tion bear close identity to pre-Albian Jurassie and Aptian miospores suggestion similarity in plant composition be-tween the Albian plants and Jurassie and Aptian ones. The impoverished nature of spores and pollen is attributed to distance of the depocentre (the Gault Sea) from the vegetational source and to a little extent water depth for D. Habib (6) found similar forms in abundance in very deep water in Bahamas. Even though the age of the sec-tion is not doubt, the study has shown that similar
pa-lynological assemblage are present in Albian abyssał
deposits in Bahamas and Wissant in France. ACKNOWLEDGEMENT
This work was funded by a Junior Feilowship Award from the University of Nigeria, Nsukka, Nigeria. The work is a part of a Ph.D. thesis at the University of Lon-don, King's College, Strand, LonLon-don, United Kingdom.
I
ain
therefore grateful to the sponsor of the project andthe authorities of King's College for their assistance and supervision. Dr. J.B. Richardsan and Dr. J.M. Hancock supervised the palynology and stratigraphy aspects of this work respectively. The manuscripts were read by Dr. C.E. Nnanedu and Dr. I.P. Grajaka and I thank them for their suggestions.
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7. H a n c o ck J.M. - Transgressions of the
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8. K e m p E.M. - Aptian and Albian miospores from
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9. K e m p E.M. - Probabie angiosperm pollen from
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17. P r i c e F.G.H. - On the Gault of Fo1kestone. Quart.
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18. P r i c e R.J. - The stratigraphical zonation of the
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STRESZCZENIE
W utworach albu południowej Anglii stwierdzono
występowanie 27 gatunków spor i pyłków. W pracy
prze-dyskutowano zubożałość palynomorfów albu i
porów-nano je z formami jurajskimi i apckimi. Występowanie
sporów i pyłków skorelowano z zonami amonitowymi
ustanowionymi w profilu Folkestone.
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