34 
exist (in the Early, and Middle to Late Maykopian respectively). 
These will be reported in detail in a future publication. 
Palynological evidence indicates that the Maykopian is a 
regressive unit characterised by upwardly-increasing terrestrial 
input (upwardly-increasing pollen and spore content). 
Micropalaeontological and sedimentological evidence also 
indicates shallowing upward. 
Tarkhanian to Konkian (Figs 8—10) 
These stages have collectively been correlated with the Badenian 
of Central Paratethys (see, for instance, Steininger et a/., in 
Royden & Horvath, 1987). The Badenian is Middle Miocene 
(planktonic foraminiferal zones N8—?N12 (see, for instance, 
Papp et al., 1968, Rogl et al., 1978 and Papp & Schmid, 1985); 
calcareous nannoplankton zones NN5—NN7 (see, for instance, 
Rog] et al., 1978, Papp & Schmid, 1985 and Meszaros, 1992)). 
Palynologically, it is locally characterised by mangrove elements 
(Nagy & Kokay, 1991). 
The base of the Badenian (the Moravian sub-stage of Papp et 
al. (1978) (Lagenid Zone)) is defined at the first appearance of 
the planktonic foraminifer Praeorbulina (Zone N8) (Papp et al., 
1968). The first appearance of the ancestral form Globigerinoides 
bisphericus, which defines the base of Zone N8 (Blow, 1969), falls 
within the underlying Karpatian (Cicha et al, 1967). This 
biostratigraphic control indicates that the base of the Badenian 
can be correlated with the 16.5Ma (glacio-eustatic) sea-level 
low-stand of Haq et al. (1988) (Fig. 5). 
The middle part of the Badenian (the Wielician sub-stage of 
Papp et al. (1978) (Sandschaler Zone)) is characterised by 
marginal marine sediments (including evaporites). This 
R.W. JONES AND M.D. SIMMONS 
regressive sub-stage can be tentatively calibrated against 
planktonic foraminiferal Zones NIO-N12 or calcareous 
nannoplankton zones NNS—NN6 (see, for instance, R6gl er al. 
(1978) and Papp & Schmid (1985)). The onset of regressive 
conditions can be tentatively correlated with the 15.5Ma 
(glacio-eustatic) sea-level low-stand of Haq et al. (1988) (Fig. 5). 
The regressive coarse clastics of the Chokrakian and 
Karaganian in Eastern Paratethys also appear to be associated 
with this event (though they could be associated with a separate 
tectonic event). These clastics constitute important reservoirs in 
the Indol Kuban and Terek Caspian Foredeeps (Ulmishek & 
Harrison, 1981) and in eastern Azerbaijan (Ali-Zade et al., 
1986). Chepalyga (1985) calibrates the Chokrakian and | 
Karaganian against magnetostratigraphic polarity epochs 
15-12, while Zubakov & Borzenkova (1990) calibrate them 
against polarity epochs 16-14. 
The top of the Badenian (the Kosovian sub-stage of Papp er 
al. (1978) (Buliminid-Bolivinid Zone)) is defined below the last 
appearances of Globorotalia mayerilsiakensis (N14) and 
Globigerina druryi (N15) (Papp et al., 1978; Papp & Schmid, 
1985). 
Details of Tarkhanian to Konkian stratigraphy have been | 
discussed by Andrusov (1884), Bogdanowicz (1950a—b, 1965), 
Shishova (1955), Gasanova (1965), Mamedova (1971), 
Azizbekov (1972), Lupov et al. (1972), Dzhabarova (1973), 
Cicha et al. (1983) and Ali-Zade et al. (1986). A monograph of 
polymorphinid foraminifera of this age from Georgia was 
published by Dzharelidze (1977). 
In eastern Azerbaijan the Karaganian and Konkian, together 
with the overlying Sarmatian and Maeotian, are collectively 
referred to as the Diatom Suite (because of the presence of 
we 
Regional (Khadumian) 
Source 
Early Oligocene Platform 
Carbonates in Armenia 
Fig.7 Palaeogeographic reconstruction, Early Maykopian (Early Oligocene). Solid line indicates relatively well constrained, dashed line poorly 
constrained shoreline. Ticks on landward side. The location of the Maykopian stratotype is indicated. 
