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Except for shape, laminae in these stromatolites are similar to those occurring in the upper part of the underlying unit. These stromatolites commonly form stromatolitic bioherms, which range from 5-20 m in diameter and are separated by 1-2 m wide channels filled with thinly bedded finegrained limestone (probably eroded from stromatolitic mats) and silty and sandy dolomitic limestone. Stromatolite- debris beds of the type that occur in the underlying Lower Baicalia Unit are not present in this unit.

The early phases of attenuation and basin subsidence were accompanied by extensional growth faults, some of which may have involved thinned basement, particularly over and on the flanks of the thermal uplift. Grabens and half grabens formed in the western part of the basin during this extensional period and became depocenters for early Belt sediments that were intercalated locally with submarine volcanics and coeval sills and exhalative metal deposits. Basal, coarse-grained clastics were deposited along parts of the north, east, and south margins of the basin.

Low energy, not shallow water depth, probably is an important factor for the development of Conophyton (elsewhere Conophyton has been interpreted as a deeper water form). Alternatively, increased resistance of the stromatolitic laminae to breakup could have played on important role in the formation of Co nophyton, as peaked growth surfaces could resist breakup if they were stronger (perhaps through increased calcification). Motile filamentous microorganisms probably played an important role in the formation of conical laminae as well as the ridges in columns with lanceolate, sphenate, and stellate laminae in transverse sections.

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