Table Of ContentOn the biostratigraphy and cyclostratigraphy
of the Moscovian Stage in the type area
Marya Kh. MAKHLINA
Geocentre Moscow,
Varshavskoye shosse, 39a, 113105 Moscow (Russia)
Marya N. SOLOVIEVA t & Nataiia V. GOREVA
Geological Institute of the Russian Academy of Sciences,
Pyzhevsky per., 7, 109017 Moscow (Russia)
Makhlina M- Kh., Solovieva M. N & Goreva N.V. 1997. — On the biostratigraphy and
cyclostratigraphy of the Moscovian Stage in the type area, in Crasquin-Soleau S. & De
Wever P. (eds), Pen-Tethys: stratigraphie corrélations, Geodiversitas 19 (2) : 235-245.
ABSTRACT
Moscovian Stage deposits are widespread in Russia. The stage wus cscablished
in 1890 by Nikicin. It is subdivised in four horizons: Vereya, Kashira,
Podol’sk and Myachkovo. The subdivisions of the stage are based on studies
of brachipods, foraminifera, conodonts, ammonites, bivalves, rugo.sans and
KEYWORDS
Moscovian, plants. In thi.s paper, new data are due to the correction of the standard sec¬
Carboniferous, tion of chc Moscovian Stage and its nc\v interprétation. Cyclostratigraphy
biostratigrapliy,
analysis based on the geological histoiy' of the région and its eustatics is a new
cyclostratigraphy,
Moscow Synciine. aspect of the rcscarch presented in this paper.
RÉSUMÉ
Les dépôts du Moscovien sont largement répandus en Russie. Cet étage a été
défini en 1890 par Nikitin. II est subdivisé en quatre horizons : Vereya,
Kashira, Podofsk et Myachkovo. Les .subdivisions de l'étage sont fondées sur
Tétude des brachiopodes, foraminifères, conodontes, ammonites, bivalves,
MOTS CLÉS
Moscovicn, rugueux et plantes. Dans cet article, les nouvelles données proviennent de la
Carbonifère, révision de la coupc stand.ird de l'éragc et de .scs nouvelles interprétations.
bio.stratigraphic,
L’analyse cyclosiratigrapliiquc fondée sur l'histoire géologique de la région et
cyclüstratigraphie,
synclinal de Moscou. de son eustatisme est un nouvel aspect de k recherche présente ici.
GEODIVERSITAS • 1997 • 19(2) 235
Malchlina M. Kh., Solovieva M. N. t & Goreva N. V.
The Moscovinn Stag;e deposits as well as the were caused by die discovery ofa gap in the stra¬
Middle Carbonîfcrous oncs as a vvhole are wides- totype section of the Kashira Horizon, where
pread in Russia and minerai deposits, including deposits of the Tsna unit, estahlished by
oil and gas, arc rather common in these sédi¬ -Solovieva (1984, 1986) in the fsna River basin
ments. Subdivision and corrélation of the (Ryazan-Saratov dépression) in the easiern part
Moscovian polylacial deposits connected with of the Moscow Synoclisc, arc absent. Cyclostrati-
different climatic zones (subtropical and boréal) graphical anal^'sis of the Moscovian Stage based
represent tJic esscncia! elernetu of geological on the geological history of the région and its
mapping and exploitation. Icndency lo adéquate eii.stadc tectonics is rhe new aspect of the rcscar-
reliability, précision of stratigraphie scale.s and ch presented in rhis paper
high degrce of corrélations achicvcmcnc causcd
the necessiiv to reinve.stigate of the stage and l'hc Moscovian Stage in rlie type area îs represen-
substage stratotypes. led by marine deposits. Le hy continuons sériés
The Moscovian Stage was establislied by Nikiiin of transgressive deposits (130-150 m rhick), in
in 1890 in tbe vicinity ol: Moscow. l'he upper which sands and clays are graduallv rcplaced by
limit of flic stage was dcfined at rhe base of clayey and pure limesroncs, Subhorizontal hed-
Gzhelian limcstoncs. ding and cycticic)^ of deposits give opporrunjt) to
The Moscovian, according co the ideas of Ivanov idenrify and follow up horizons, formations and
(1926) who had estahlished the fundamental relatively smaJl subdivisions (suhfbrmations and
principles of the modem views on ihe volume of memhers) in this région, and to identify cycles of
this stage and its subdivisions based on the stu- different order.
dies of the deposiiional sequence in the Southern If che CnrbonifcroLis S)^tcm is considered to be a
parc ot the Moscow Syneclise, was suhdivided cycle of the third order, Middle and Upper
into four horizons: Vcrcya. Kashira, Podolsk and Carboniferous (Pennsylvanian) are c)'clcs of the
Myachkovo. The Tegulifera Horizon (the fourth order. The Middle Carboniterous corres¬
Kasimovian Stage) was considered to be a part of ponds CO a tcccono-cLisratic cycle of the flfth
die Upper Carboniterous. Faunal assemblages of order, tlie Moscovian and Kasimovian stages to
che Moscovian as a whole, as well as rhose of its cycles' of che sixih order (Table 1). According to
subdivisions based on studies of bradiiopods, Tilebomirov (1988), the lattcr includes the chree
foraminifers, conodonrs, ammonites,, bivalves, units correspondiiig to three phases of che trans¬
rugosans, plants, are rekuivcly well known, zonal gression: initial (a), maximum (jî) and terminal,
scalcs being estahlished on the hasis of some of or regreS-sive phase (y). Cycles of the sixth order
these studied groups. Numerous publications are may be complété or .shortened, rhe former
devored to che Moscovian Stage in the type area, consi.sting of chree cycles of the seventh order,
which mosr important are rhose by Ivanov che lattcr of two cycles oi the samc order, the ini¬
(1926), Ivanova &c Khvorova (1955), Raiiser- tial phase being absent- These cycles could be
Chernousova et ai (1951). Some papers are followed up in different faciès throughout a
published during the last 20 vears by Shik rcgioiit and cheir forinacion corresponds lo the
(1971), Makhlina (1972, 1976), Makhlina & maximum lectono-eustatic changes of basin
Shik (1983), Makhlina et al. (1984), Goreva levcl. 'Hie A/a, Vereya and T.sna subdivisions
(1984), Solovieva (1984, 1986). apparenily cotre.spond to rhe cycle of the seventh
New data included tn rhe présent paper w'crc order, or to the initial phase of the transgression
obtaincd by the correction of the standard sec¬ (tï) (Table 1). l'he combiacd Ka.shija, Podolsk
tion of the Moscovian Stage and its new inter¬ and Myachkovo horizons correspond to the cycle
prétation. of che seventh order, or to the maximum phase
The lower houndary of ihe Moscovian Stage, of rhe transgi-ession (P), whercas chree horizons
according to the iraditional views, coïncides wirh of rhe Kasimovian Stage of rhe Upper
rhe lower boundaty of the Vereya Horizon. Carboniferous correspond to a régressive phase
Changes in the standard section interprétation (y). Within the cycles of the seventh order there
236 GEODIVERSITAS • 1997 • 19(2)
Bio-cyclostratigraphy of the Moscovian Stage
Table 1. — Subdivision of the Moscovician of the Russian Platform.
Régional Local scale Cyclostraligraphy scale
scale Moscow Synclise order of cycles 1
IX VIII D IV III
Horizon Formation Subformation Member Horizon Substage
(Formation) stage CTE0>On9.
ri CO
Voskresensk
n
Krevyakino Krevyakino Suvorovo Krevyakino Krevyakinian y movia pper
zi u
a
K
Myachkova Peski Peski Myachkovian c
re
Noviinskoe Noviinskoe
Shehurovo Shehurovo c -
Podorsk Podol'sk Ulitino Ulitino Podolskian (0 c
Vas'kino Vas'kino (32 <u <0 a,
Smedva Smedva Smedva > BH B
Rostislavr
O O B
Lopasnya Lopasnya Lopasnya Kashirian P O
Kashira Kashira Khatum pi w CO
Nara O c
Nara Polustova Nara _c
Gora eu
Tsna Tsna Tsnian? O
a3 1 1
Upper (cid:9632) 1B
Vereya Vereya Vereyan a (cid:9632)
Lower Shat a2 (cid:9632) 1
Melekess Aza Aza al (cid:9632) (cid:9632)
are smaller cycles - those of the eighth order, cor- environmenrs. Periodicity in the distribution of
responding to separate horizons (substages in the faunal assemblages, which always show maxi¬
proposed cyclostracigraphic scale, Table 1) and mum diversiry in a transgressive part of a cycle
those of the first order, corresponding to subfor¬ and low diversit)'^ in its régressive part (Makhlina
mations (hori/.t)ns in the proposed cyclostrati- Sbik 1983), is a charnctcristic fcaturc of ail
graphic scale, Table I). simultancoiisly formed polyfacial stratigraphie
units corresponding to the cycles (Figs 1-3).
Every stratigraphie unit of any rank can be sub- Boundaries between tbese units correspond lo
divided iiuo two parts: lower^ corresponding to historico'geological changes of sédimentation
ihe transgressive pha.se of sedimentarion, and patterns, i.e. to changes in abioric environment
upper, corresponding lo ihe régressive phase. taking place simultaneousiy in the wholc région
Contemporaneous stratigraphie units of different (Makhlina 1996).
faciès, which wcrc formed in the paleobasin as a The Jnain criteria for distinguishing and cracing
latéral sequence of rocks rcflect, ncat-shore, per- ot transgressive-regressive cycles in which combi¬
iferal, shallow-water and relatively deep-water nation form stratigraphie units (formations, sub-
GEODIVERSITAS • 1997 • 19(2) 237
Makhlina M. Kh., Solovieva M. N. t & Goreva N. V.
formations) are ihe follovA'ing: sedimcntological N. bttsslcri, Dfplognctthodus adoradoensis-,
and faunistic content, features of texture, perio- D. orphnnits, Streptognathodtis parviis.
dicity in rhe distribution of ail groups oi iauna in According to Solovieva (1984) and Alekseev
the section, as well as blostratigraphic;d characte- (1994), the Vereya Formation sensu Ivanov
ristics for the définition of the gcological age of (1926) is only charaeVerized by the yVlyutovo
the units. ’l'hc sufficient methodical signifîcance fïisulinid and conodont assemblages. The over¬
of the lirhological-palaeoecological criteria, ela- lying and underlying Shat and Ordynha mem-
borated by Osipova & Belskaya (1967). should bers ( Fable 1) do not contain any orber tàunisric
be emphasized in this respect. complex except Alyutovo age.
Leaving aside the problcm of rhe lower boundary
In the standard of the Moscovian Stage, the posi¬
of the Moscovian Stage, chat is stÜl discussed
tion ahove the Vereya Formation in the case of
(Solovieva 1986; Aleksecv et ai 1994), let us give
normal scquence is occupied hy rhe Tsna unit
brief characterisrics of the stratotype sections of
distinguished hy Solovieva {1984, J986). Tn rhe
the horizons (formations, subformations), Le. of
stratotype section (Yambirnoye Quarry, Ryazan
units of the régional and Joca) s'cales ol the
région, Fig. l'H) it is represented by inierbcd-
Moscovian Stage, accepted in Russia
ding ol dcrrital and doloniitr/.ed finc-grained
(Anonymous 1988, Table l).
limestones with greenish clays and marks, rarely
with micro-grained dolomites (Fig. 2-11). The
The Vercya Horizon (Formation), in order to
tliickness of rhe subformaiioii in the stratotype is
reinvesrigate the stratutype, was studied ncar the
16.5 m (Table ty Local Scalc, 1988).
village Alyutovo on the righc bank of the Pronja
Deposits of the Tsna Subformarion correspond
river, where it is lying ciansgressively on Lower
to the Zone Aljutonelln pritcoideas HctnifitsuUna
Carboniferous deposits (Solovieva 1986)
volgeyisis. l'his typical forantiniferal asscmbhige,
(Fig. 2-1). Red sand and clays, glauconite Sând-
characteri/ed by a high dcgrec of similarity m ail
stones can be found in the base ol the section,
régions where the.se deposits arc represented (rhe
crinoid-bryozoan sandy limestones with forâmi-
Russian Plaiform, rhe Douces Basin,, the
nifers, as well as intoibedding of crinoid lime¬
Cisuralian Dépression, Urals, Tien-Shan, etc.),
stones, variegated c!ays> maris with brachiopods
iücludes the follov^nng species: Schtibemila gTiici-
and bryozoans overlying them (Ivanova &
lis znensis^ Sch. galinae, Ozawainella digitnUsy
KTvorova 195S). l'he chickness of che formation
ProfnsulificdJa prisen tîntanica^ P nnrûtovensis,
in this section is 10 m, and in the région ir
P jmta^ Taitzehoella prolibrovichi, T. pseudolibro-
changes from 10 to 3? ni. The Vereya Formation
Vîckd, Aljutovella parasaratovica^ zl. ùuralovtca,
is subdivided into rwo subforniarîons, lower and
A. priscoidca^ A. znensisy Hemîfusidina dutkevîchi,
Lippcr (Anonymous 1988). Solovieva (1986) pro-
H. volgemis.
posed the foraminileral Proftisiinella cavis,
Aljutovella aljutovica. AL artificirxHs Zone. The
typical assemblage of the Vereya Horizon
(Formation) ts fcprcsented by tho following spe-
cies of foraminifers; Eostaffelln mutabilis,
Schubertella püuçhepuuay Psvudosmffclla suhqua-
dratUt Profiisulinella cavis, P parvn^ Aljutovella
aljutoviça, A. artificialis, A. scclvevatictu
A. euhnea, ehn^ntft.
Deposits of the Vereya Horizon (Formation) cor¬
respond the conodont IdiognatiHndes tubercu-
TO
lattis^ !d. mitrginodosus Zone. Characccristic
species of the zone arc Idiogriathoides dnnhassiens.
Id. shnuxtus^ Id. fossatuf. ïd, ein'rngatus^
FfG. 1. — Location map of the stratotype sections (l-X) of the
Idiognathodus incurvusy Neognathodus atokaensis-, Moscovian Stage (for the list of the sections, see figures 2. 3).
238 GEODIVERSITAS • 1997 • 19(2)
Bio-q^clostratigraphy of the Moscovian Stage
According to thc prdimlnary investigations, ihe rnoelleri, H. kashirka communis, H. splcndida,
l'sna Subformatîon corresponds ro the tonodonr Beedeina ozaivai-, B. paraozaivah B. pseudoelegam.
Neogtmthodus bathrops^ Streptognathodus tramiîi-
The Rostislavf member consists of two parts.
vus Zone. J'iie lowcr boundary is defined by rbe
The lowcr onc is represented by interbedding of
entry of Neagvathodus boihrops, the upper one by
clays and limestones, or by unfossiliferons days,
the incoming ot Streptoguathodus disi^ectus.
or by dolomicic maris (bed 23, Fig. 2-IV), the
Deposits arc characterized by an inipoverished
upper one by sands, aleurolites, sandstones and
conodont complcx. Typical spedes are as follows:
conglomerace (bed 21, Fig. 1-V), The lower part
Neognathodîis bothraps^ Streptügndthudus pürinis^
corresponds to a régressive phase and terminâtes
Idiognathodiis delicatus-, Id. cd^llqitus, Diplo-
the kopasoy.a Snhformation, the upper part,
gnathodus colonidoemis.
being the transgressive one, corresponds to the
Deposits of che Tsna Subformaiion hâve a spotcy
base of rhe Smedva Subformarion.
distribution due to the transgressive bedding on
it of thc Kashira Horizon that corresponds to the The Smedva Subformarion, or according to
beginning of maximum transgression ((îj, Ivanov (1926) “dolomites of Smedva”, contains
Table 1). micnjgraincd dolomites and dctrital limestones
(Fig. 2-V). U was referred to the Podol.sk
The Nara Subformation is represented by an
Horizon by Ivanov and Solovieva, many of the
interbedding of poorly coloured micrograincd
subséquent auihors assigned tbi.s subformatinn to
limestones and dolomites wiih biodetrital lime-
the Kashira Horizon. “Dolomites of Smedva'
srones and clay seams. The thickness of thc
represent lagoonal rocks characteristic of a régres¬
deposits eau reach 28 ni {Fig. 2-II1). Materials
sive phase. I hls environment was imfavorablc for
available give ati opportuniiy lo substantiate ihe
fusLilinids. dliaC is why deposits of the Smedva
récognition of thc local Hemifiisulhm kushiricUy
Subformation are very poorly characrerized by
H, moellert^ Becekina pscudoelegans Zone. In the
this group of tauaa. The Lopasnya and Smedva
eastern sections of the Southern part of rhe
subformations correspond to the conodont
Russian Platform chcrc arc numerous Neo-
Neognathodus medadultirnus^ Streptognathodus
stajjellu, Profusnlinelta pseudolibrovichi, Pr. eoli-
dissectus Zone. The lowcr limit of the zone Is
brovichi. Pi. syzranicas Pr. mtHahiUs^
defined by lhe incoming ot Neognathodus meda-
Heniifusulim kashirka. H. pseudobochi. H. mocl-
diiltirniis^ the upper one by the entry ot
leri, Beedchm hontu B. Qznwau B. pseu-doelcgatis^
N. medexultimm. Characteristic spccies are as fol¬
B. d(. proQZiiWiü^ B. kayi. The Nara Subtormation
lows; N. hothrops^ N. medadultiinus, N. colom-
corresponds to thc conodont Ncognathodiis
biensis^ Idiognathodus obliquus^ L delicutus^
bothropSy Streptognathodus disseetns Zone. It is
I. robustiLu Streptognathodus dissectus, Diplogna-
characicrizcd by ihc following species:
thodus coloradoerisis. This zone can be subdlvided
Ncognathodus bothrops^ N. kashtrieiists, Sti: dissec-
into two local subzones, each with a characterls-
tus^ Str. parvus. Diplognathodus voloriidoensis is
tic assemblage: Suh/.one Neognathodus bothrops»
very common.
N medadultimus, corresponding to thc Lopasnya
The overlying Lopasnya Subformarion is repre¬ Sublormation, and Subzone N. medexultirnus
sented by interbedding of pinkish and greenish corresponding ro the Smedva SubRirmation. Ttic
limestones, dctrital, micrograincd, with cherts, volume of tlic former sub-zone is designated by
variegated maris, more rarely dolomites. Its the coexistence of A^. bothrups and N. medadultk
thickness is 15-30 ni (Fig. 2-1V)- The subforma¬ mus, the characteristic complex lieing represented
tion corresponds to thc local Moellerites lopUs- by N. hotbrops, N. medadultufius, Strepîognd'-
viensis, Beedeina ozawai, Fusulinella sahpulchni thodus dissectus, Idiognathodiis oblitjuus, l he
Zone (Solovieva 1986). The Ibllowing complex volume of lhe latier subzune is designated by the
is characteristic: Ozawamelht stellae., Pmîellilprae- présence of Neognathodus medexultirnus, Stiepto-
cuTsor paraventricoui., F. praetypica, Neostajfella gnathodus dissectus, Idiognathodus obliquus,
larionovae, Fusidinella subptdchray Hemifusulina L robustus.
GEODIVERSITAS • 1997 • 19 (2) 239
^3 ^4 ^5 ^6 ^7
9 10 11 12 hr^ 13 14 l^-:-:;J ib 1'®^ 16
I & I 17 I O I IB l^ I 19 I ^'i ZO I cÿ ) 21 \A I 22 I ü I 23 |g<l 24
r~0n 26 1 f i 26 I 1 27 f-*~^ 20 l'^l L-l 29 l*^»l 30 I ] 31 | lil| | 32
33 IV^I 34 liTÜIll 3B
Fig. 2. — Sections of the Moscovian Stage (Veroya. Tsna and Kashira beds); I. outcrops near ihe Alyutovo village, right bank of the
Pronja River {Solovieva 1986), lectostratotype ol the Vereya Formation; II, Yambirnoye Quarry near the Yambirnoye village, left bank
of the Tsna R'ver (Solovieva 1986'/; the Tsna Suoformaîion holostralolype; III. outcrops along the Oka. Nara. Protva. Besputa rivers:
section oî the Nara Subtomiation of the Kashira Formation (ivanova » Khvorova 1955, fig. 13), !V, ourcfop near ihe Lapmo village at
ihe left bank ot the Lopasnya River (near the Knatun village) (Solovieva 1986): siratotype ol the Lopasnya Subiormatton. layer 1.
Khatun member: layer 23, Rostislavrmember. the lower part; V. outcrops along the OKa. Nara, Protva. Besputa rivers; sections of
the Smedva Suütofrnation ot the Kashira Formalion: layer 21. RostislavI rnember, lhe upper pan (Ivanova & Khvorova 1955,
fig 13).
Legend for figorys 2*3 Depos«ts 1-16:1. Kmestone; 2. d&tr*ta! ai biomorphlc-detriial limêslone- 3, siuôge limestone; 4. microg^ained
limestone; 5, coprolilc-dclnlal limestone. 6. lime sanostone, 7. dolomite; 8, miçrograined dolomite; 9. clayey limestone: 10. mari: 11,
ciayey dolomite; 12. dolomite mari; 13. dolomitized limestone; 14, Time and aoiomlte ctay; 15. sand sill, sandstone; 1B. fragments oi
chert and limestone. Fossils 17-29; 17, foraminifers; 18, brachiopods. 19, solllary corals: 20, colonial corals; 21, bivalves; 22. gastro-
pods: 23. Dryozoans: 24. fishes. 25. chnoids; 26. echinoids; 27. algae: 28. aigae Ivanovia tenuissima; 29, traces of mud-eaters;
Secondai^ alterations, structure and other signs 30-35; 30. cherts: 31. caverns: 32. stylioliies: 33. cross-beddlng 34. limestone brec-
cia. 35. gap
l'he Podolsk Horizon (Formation), a maximum rcpre-scntcd m;iinly by biomorphic limestones
phase of the Moscovian transgression (p2)» is with seams of miçrograined dolomites, greenish
iAr\ GEODIVERSITAS « 1997 • 19(2)
Bio-cyclostratigraphy of the Moscovian Stage
mari and clays; the total thickness is 25-40 m. compicx is as fbilows: OzMwatnella kumkhoverisis,
Three subtormations can be identified within NeostaffelLi rosm^zein^ N. sphueroklea^ Taitzebeella
this formation. librovitchi aieliidy FusuHnella colaniae,, Hemi-
fusulina splcndida, Bt-rdeina elegans, B. omwai,
The lower one (Vas’kino Subformation) is repre-
B. elshanica vaskinensh, Putrella triangnU-.
sentcd by miciograined Jimcstoncs and dolo¬
mites with biomorphic'dctrital limestone seams; 1 he overlying Ulilino Subformation is similar to
the thickness is 7-12 m (Fig. 3-Vl). At the base, the Vas'kino in the sedimeniological aspect but
there are conglomérâtes and maris that could be differs m rhe présence of limestone seams with
traced regionally. The Vas'kino Subformation the algae Ivanovia termissinut. The thickness of
corresponds to the tusulinid FusuUneUa colaniacy the deposits is 12-13 m (Fig. 3-VIT). The sub-
Beedeina elegans Zone. The characteristic formation corresponds to the local FusuHnella
Fig. 3. — Sor.tlonç of the ^/1o8COV^* Stage (Podoi'sk. Myachkovo norirona): VI soriionK m mo nasm ot ihe Oka ffive» east of ihe
Kashira towo, near Bolstioyo Huno village, pogoM Rosttftiavi’. and noar Vas'kino village, section ol ihu Vas’Kino Subformatloo of (he
Podol'sk Formation (Ivanovan & Khvorova tP-W. np ?0i VII, Quany near ihü town Podoi'sk: ntraiotype ol the Podoi'&k Formariun
(Ulltino Süblormaiion) [Ivanova & Klivurova 1ÔS5. fig. VHI, Üuarry ooarthe lowo Potioi'i^k. atraiolypao* ÜiaPodolBk Formation
(Shehurovo Sublormation) <lvanova & Khvorova 10W, (ig 23) «X, Ooairy |(ié Ujwn Podolsk hvpostratotype ot Iho Novlinekoe
Subformalion of (hr? Myachkovo Formation (Ivanov;? fi Klivorova 1955. fig. 23); X. Atanusiovo Üuarry noar the Atanaslevo villagH on
the nght bank ni the Moekva River, tteclion of Hie Mvachkovo-KrovyaKino boundary tayors (Middlft/Upper Oarhoni/erüus boundaryl;
layer 6, “lower conHlomarate'*: lay^r 7, dolomite oi Turaovo"; loyer 8..'0trmH8l)a". lay^r fi. aharstia . layer TO, upper conglome-
rate". Hypostratotype of the Peski Subformation of the Myachkovo Formation: it is near Peski raiiway station, on the left bank of the
Moskva River (Makhlina étal-1972, 1984).
GEODIVERSITAS * 1997 • 19(2) 24 I
Makhlina M. Kh., Solovieva M. N. t & Goreva N. V.
vozghalemk^ Fusidina Utinensis Zone, the follo- Pidchrella pulclmu Hemifimdina bocki, FI. stdbilis,
wing complcx being considered as a cbaractcris- Fusidina cylindrica,
tic one: Fusiella putchella, Neostaffella ozaumi,
The upper one, Peski Subformation, is represen¬
Ozawainella mosquensis, FusulinelLi vozhgalensis,
ted by biomorphic-detrital limestone with lenses
Hemifusulina stabilis, H. polasnemîs, Fusulina
of lightcoloured maris and clays. ‘‘Turaevo”
ulitinemh, F. panconeîish, Purtrlla bmzhnikovae.
micrograined dolomite at the top accomplishes
'l’hc uppermost part of the Podolsk Formation is the maximum phase of the Moscovian transgres¬
identified as the Shehurovo Subformation repre- sion. The thickness of the depo.sits is 7-15 m
sented by dolomites* biomorphic limestones wich (Fig. 3-X). L^eposits of chc Peski Subformation
greenish mari and clayey limestone seams. correspond to the local FusuUnella podolskensis,
Limestones are ofren dolomiti/ed and siliceous. F. cylindrica domodedovi Zone. The data avai-
The thickness of the deposirs is 8-12 m lable, especiaJly those concerning fusulinid distri¬
(Fig. 3-Vni). riie Shehurovo Subrormaiion cor¬ bution (Makhlina et al, 1972) givc ân op-
responds to Becdcina kameyisis^ Pmrrlla brazhn 't- porcuniçy to indicatc complcx typical of the
kovae, Ozawainellu ynosquensis Zone with deposirs of chc I*eski Subformation: Schubertella
accompanying characteristic complex of mjachkovensh. Ozaivairiella mosquensis,,
FusuUnella hockiy F. îwzghulensis, B. elegans^ FusuUnella bockh F yata, F podolskensd^ F. hele-
B, shellunem, B. elshanka, nae^ F. mosquensis, F. kumpaniy Hemifusulina
Deposits of the Podolsk Horizon correspond co bocki, Fusidina cylindrica domodedovi. F mos-
the conodont Neognathodus nicdexultimiis, querysis, F. mjachkovcyîsis^ F pachreiysis^ F fortissi-
Idiognathodm podobki^nsis Zone. The lower limit ma.
of the zone is deflned by the encry of rhese two
The Myachkovo Horizon (Formation) corres¬
species, the upper onc by the îneoming ol
ponds to the conodont Neognathodus roundyij
Neognathodus roitndyi. The conodont complex as
Streptogyiathodus cancetlosus Zone. The lower
a whole is not characteristic cnough, the lollo-
limit of the zone is deflned by the entry of
wing speciCvS being typical*. îdiopiathodiis podoF
Neogyiarhodus ifum{q!ialh^ N, rouyidyi^ chc upper
skensis, L nuigtiifictis^ l. delicatus^ Neognathodus
one by the incoming of S. subcxcelsusy
medadulîitynis^ N~ medexultimus,
Idiognathodm fssheri and by the disappcarance of
Neogtiathodiis spccics. Index species are domina-
rhe Myachkovo Horizon (Formation) accom-
cing in this complex, N» ynedcxultinuiSy N inae-
plishes the maximum phase of the Moscovian
quLtleSy (dfognathndm dehcant<, f. rrigonolobatm
transgression ((3^,). Tt is represented by biomor¬
being characteristic ones. 'l'he zone is suhdivided
phic limestones with micrograined dolomite
into rvvo parts considered noivadays ro be local
scams and Ughtcolourcd mari Icnses. The total
subztmes. The Noviinskoe Subformation corres¬
thickness ol rhe deposirs is 17-37 m. The forma¬
ponds tn the Neognathodus ifîaequales Subzone,
tion is divided into rvvo subfotmariuns.
charactcrizcd hy tlie acme o( the index spccies.
The lower one, Novlinskoc Subformation, is The Peski Subformation corresporid.s to the
represented by varions limestones (derrital, bio- N, roundyi Subzone, i.e. to the period of
morphic-detriial) with micrograined limestone N. vQundyi mass development and incoming of
and dolomite seams, coral-fusulinid limesStones N. dihitatiis •SiVi.à Idiognathodus trigyniolohatus.
being typical of its lower part (Fig. 3-IX). The
thickness ol die deposits is 10-23 m. Deposirs of The jifïsiiTon of the upper houndary of the
the subformation correspond to Fusnlinella hockty Moscovian Stage, i.e. the Middle/Upper
E mra, Beedema samarica Zone. The characteris¬ Carboniferous, is .srül discassed at présent time.
tic complex indudos SchubertelLx myachkovernis^ rhis houndary was establi.shcd by Ivanov (1926)
Fusielta typka, NeostaffelLt pnradoxa, N. sphaeroi- in outerops and quarrics along the Moskv^a river
dea, Fusulinella bocki, F. bocki paucheptata, and its triburaries (in Myarhkovo, Suvorova
F fluxa, E mosquensis, E rara^ Beedeina samarica^ Gora, Krevyakino and other localities). Ail these
242 GEODIVERSITAS • 1997 • 19(2)
Bio-cycloscratigraphy of the Moscovian Stage
localities artr connected to a scparate synsedinienc- Conodom distribution in rhe boundary beds
ary élévation in the Moscow zone of élévations demonstrate.s thaï the "garnasha”-"sharsha** beds
and are characterized by varying fades of rhe should be a.ssigned to the Kasimovian stage, i.e.
boundary beds, as well as by numerous erosional to rhe local Subzonc Idiognathodus arendti of che
surfaces with an intraforinaiional conglomerate Streptogtmthodus oppletus Zone (che Krcv}^akino
incerbed. Some marker beds traced by Ivânov Horizon). The lower limit of the .subzone is dofi-
(1926) in the boundary beds in this région got ned by the incoming of Idiognathodus arendti,
their own naines: bed 7 - *‘svinyâ'\ or *^dolomite 1. flshert. Sp'eptngfvzthodtts sttbexcelsiu, S. oppletus,
of Turaevo” (Makhlina et ai 1972) (Fig. 3-X) - che upper one by rhe entry of S. sugittaüs and the
lightgreen argillaceous mictograined dolomite; disappearance of Idiognathodus trigonolohutus.
bed 8 - ''gamasba" - interbedding ol green, red Characteristic species are as follows:
clays and maris, limestones, sonietiines with Streptogitathodus suhexcelsus, S. oppletus, S. excel-
conglomerate interheds. In some sections, chis sus, S. eaneellosus, Idiognathodus trigonolobatus,
member is replâced by dolomitic maris and argil- î. Jishert, J. arendti.
laceous limestones (Fig. 3-X); bed 9 - “sharsha" - The Lippet boundary of the Myachkovo Horizon
white mictograined nonhomogeneous “^conglo- (Formation), established on the basis of cyclo-
merate-likc'’ limestonc with caverns. stratigraphic analysis at the top ofthe "dolomite
The position of the upper boundary of the of Turaevo”, is proved not only by faunal distri¬
Moscovian Stage, according to the conclusions bution data but by also .sedimentological and
based on brachiopods and foraminifera srudies, is geochemical data. Bed-hy-bcd compatison of
changing within the interval from "the lower detrital limesrone microstructures pn the
conglomerate lu the base of rhe upper conglome¬ Myachkovo-Krev'yakino boundar)' demonsrrares
rate”, i.e. within lhe inccrval from bed 6 to rhat in the former cloddy pcllecal cernent struc¬
bed 10 on Fig. 2-X (Ivanov 1926; Ivanova ôe tures dominate, whercas in the latter (rhe
Khvorova 1933; Bolkhovkinova 1937; Rauser- .Suvorovo and Voskresensk subformations)
Chernousovâ & Rcitlinger 1954; Maklilina et ai mictograined oncs dominate. Compatison of the
1972). Further srudies of the lower conglomerate geochemical coefficients in the boundary beds
interbed (bed 6 on Fig 3-X) undcrlying "dolo¬ also demonstrates rhe différence in che quaiuitd-
mite of Turaevo ” showed that tliis conglomerate rivc contenr of microelements: in carbonate
wa.s from intrafonnatiorial origin and nor of inter- rocks and in clays and maris in the Noviinskoe
stagial one, becaosc ail thèse interbeds contained and Peski .subformaiions, ir is respccrively 10 and
fusulinids of Fusulvja tylindnea Zone, indicating 2000 time.s more, than in similar rocks of the
rhe Myachkovo (Feski Subformation) âge of the Suvorovo and Voskresensk .subforniations. This
"lower conglomcj’ate” (Makhlina et ai 1972). level, therefore, désignâtes the end of rhe
d'he complex of foraminifcrs above the "dolomite Moscovian transgression maximum phase (p^)
of Turaevo” (in beds 8-9, le. in ‘^garnasha” and and the beginning of a régressive phase (y). It
"sharsha”) is represented by numerous small fora- corresponds to the Kasimovian time, characteri-
minifers and fusulinids with a widc vertical dis¬ zed by the tcrrigenou.s supply with the micro-
tribution, Ozditvûînella atigulata, Globivalvulina elemental content, dilferent from ilie Moscovian,
ex gr. gmnulozd, Schuhertella rnjachkoveinh, by faciès variability in the zone of synsediment-
Endothym sp. among them. Recently, fcw oppres- ary élévations, followed by the érosion and pre-
sed Obsolètes obsolètes wcrc fouud in ibese beds. vailing of unfavorable environments for many
Mass Obsolètes enter above the bed 9 ('sharsha”). groups of fauna, particularly foraminifcrs
Therefore, we draw the boundary between rhe (Makhlina 1976; Makhlina eZ///. 1972).
Myachkovo and the Krev^^akino horizons (i.e. the
Middle/Upper Carboniferous boundary) at the Based on the data obiained from cyclostrati-
top of the "dolomite of Turaevo''' (bed 7 on graphical analysis of the Middle/Upper
Fig. 3-X) between the two conglomérâtes, the Carboniferous deposics in che type area, one may
lower one and the upper one. conclude that the Kasimovian/Gzhelian bounda-
GEODIVERSITAS * 1997 • 19(2) 243
Makhlina M. Kh., Solovieva M. N. t & Goreva N. V.
ry was more significant than rh^ Moscovian/ Alekseev A. S., Rarskov 1. S. & Kotionova I., 1.
Kasimovian oue, bccause the Kasimovian Stage 1994. — Stratigraphy of the I.owcr Moskovian
Subsrage (Mîddie Carbonilerous) Irom Central
represented che terminal phase of the Moscovian
Russia accurding to conodont invcstigition. Vesmik
transgression, whereas the Gzhclian Stage corres-
MGU, Scrie 4, Geologia 2; 33-46 |in Russian).
ponded to ihe maximum phase of the following. Rolkhoviiinova M. A. 1937- - Myachkovo section
the Gzhelian/Asseiian transgression (both the according to ne\^' paleoncology data, Thesis of report
Moscovian and the Gzhelian/Asselian transgres¬ in XVIU session of însirnastonal Geologiad Congress^
Moscow; 29^^ |in Russian).
sions represent cycles of the sixth order). This
Goreva N. 1984. — Conodonts of the .Moscovian
cyclostratigraphical boundaiy supports rhe views Stage in the Moscow Syneclise, .Sbornik "Paleonto-
of Nikirin (1890), who proposed to dravv the logical vharacteristics of straîoiypicul and hase
boundary between the "Moscow Sériés*' and the Carboniferous sections in rhe Moscow Syneclise^\
VIoscoAV. 44-) 22 (in Russian].
Gzhclian Stage below rhe limestone.s of Gzhel.
Ivanov A. i*. 1926. — Middle-Upper Carboniferous
Taking into account everything mentioned
dc'pofiifs nf Moscow province. Bulletin MOIP, volu¬
above, ono may corne to the conclusion thar me 4: 13-1R9 [in Rus.sian].
almost each of the subdivisions of Kashira, W.mov.i K. I. &[ Ëhvorova 1. V. 1955. — Stratigraphy
Podofsk and Myachkovo horizons (formations) of rhe Midiile .ind Upper Cjrboniferou.s in chc wes¬
tern part of the Moscow Synctlisc. Trtidy Paleon-
are characterized by zonal conodont and fusuli-
tologischeskyi Institute Acaderny Nauk USSRy
nid assemblages, and can be traced in different
Moscow, tome 53: 1-281 [in Russian].
faciès ail ûver rhe major part of the Moscow Khvorova I. V. 1953. — llvolurion of Middle and
Syneclise and other régions of the Russian Upper Carboniferous Basin in the western part of
Plarform, and aiso outside of it It gives the the Moscow Synecll.se. Trudy PIPI, tome XLill,
Moscow, 22Ü p. [in Russian].
opportunity to raise the rank of these subdivi¬
Maldilina M. Kh. 1976. — Comparative characteris-
sions and to regard them as rhe horizons (cycles
ticcof ihc structure of Moskovian, Kasimovian and
of the eighth order) of the Russian Platform tïzhelian-A.s.selian stages of the Upper Paleozoic in
Régional Scalc (Table 1). We believe also thar the Podmosküsye. Izvestya \'9JZov. Geulogia i uizvedka,
horizons estahlished by Tvannv in 1926 (the Nü. 6: 3-10 (in Russian].
— 1996. — Cyclic sti Miigraphyv faciès and launa of
Vereya, Kashira, Podol'sk and Myachkovo -
the Lower Cjrboniferôu.s (Dinantian) of the
cycles of the eighth ordci) correspond to stages, Moscow Synecli.se and Voronezh AntecUsc, in
as it has heen demonstraced by Ivanova in 1955 Rcceni Advânces in l.ower Carboniferous Geologjs
and proved by numerous data, obtained during Genlogkal Society, Spécial Publication. No. 107:
359-364.
the following ycars. Howevet. in May 1995, the
Makhlina M. Kh., Koulikova A. M. de Rourkovsky
Interdepart-mental Stratigraphie Commirtee ol
V. P. 1972, — New data aboui a detaÜed compari-
Russia dccidcd to consider horizons of rhe son of stratigraphie sections, Izvesrya VUZov^
Moscovian Stage of the Global Scale as subsrages Gtologra i razvedka. Ko. 10; 13-20 |in Russian|.
with their own n.imes. As ro rhe Tsna Makhlina M. Kh. & Shik R. M, 1983. -Cydo-
.stracigrapKic merhod for a detailed invesrigaiion of
Subformation, the problein oi ils rank still
Upper and Middle Carboniferous depo.sir.s in
remains debatable (should il be a horizon or a
Podmoskovye. Izuesrya VLlZotf. Geoîogin / razoedka.
substage?). Solovieva considered the Tsna beds to No. 2:3-14 (iti Russian].
be of a stage rank. Tt can be traced in the Russian Makhlina M. Kh., Isakova T.N*. & JouÜtova V.E.
Platform, as well as in Ticn-Shan, Donets Basin, 1984. — Upper Carboniferous In Podmoskovye.
Vestmk sbtsrntk Verhnt Carbon SSSR\ Nauka: 5-14
lirais and other régions.
[in Ru.^sian].
Nikitin S. N. 1890. — Carboniferous deposits of the
Moscow area and arlesian wau-rs in the vicinity of
REFERENCES Moscow. Trudy Gtmlogischeskyi Com., tome 5,
No. 5: 1-181 |în RussiânJ.
Anonymous 1990. — Decision of the Inter- Osipova A. I. &: Belskara T. N. 1967. — An expé¬
departmental Régional Swatigrapbic Conférence on rience of A lithologicaf-mlacoccological study of the
the Mieidlc and Jpper Paleozoic nf the Russian Visean-Namriri.in dcpo.sîts in the Moscow
Platfonn (Leningrad, 1988). Carboniferous System. Syneclise. Lithologla i polezn. iskop.. No. 5:
Léningrad, 95 p. [in Russian]. 118-142 [in Russian].
244 GEODIVERSITAS • 1997 • 19(2)
