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The Hosts of Cavity Minerals (The Deccan Volcanic Province) Chapter I I

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The Hosts of Cavity Minerals (The Deccan Volcanic Province) Chapter I I 1^-00 THE HOSTS OF CAVITY MINERALS (THE DECCAN VOLCANIC PROVINCE) CHAPTER I I THE HOSTS OF CAVITY MINERALS C THE DECCAN VOLCANIC PROVINCE ) 2.0 INTRODUCTION : A volcanic asBOci&tion defined by Kennedy (1938) includes all associated igneous rocks, may be strictly volcanic or related to the particular cycle of volcanic activity. Since very long tiue the tern plateau basalts, synonynous with flood basalts, has been in use to describe subhorizontal basaltic lava flows which nay have accunulated in rapid succession and nay have spread over extensive areas. They are generally believed to be products of fissure eruptions on a regional scale and are associated with nunerous intrusives in the forn of dykes, swarns of dykes, sills etc. having cheuical similarities with the erupted lava flows. Two types of parent magmas giving rise to flood basalts are distinguished by Kennedy (1930), namely, (i) Tholeiitic, and (ii) The olivine basalt magma. The Deccan plateau of western India, now uniformly recognized as the Deccan Volcanic Province (DVP) stands amongst the classic instances of the tholeiitic flood basalt provinces, recognised all over the World, in parallel with Columbia Snake River plains of USA together with other instances such as Keweenawan lavas of Lake Superior, South African Stromberg lavas, the "Traps" of Hew Jersy and the Parna basalts of South America. The tholeiitic lavas of Australia also belong to the same general category where enorioous volumes of tholeiitic basalt lavas were erupted on an extensive scale. A considerable interest in the study of the flood basalts of the Deccan has been regenerated during the past two decades on account of their period of eruption (65 ± 5 u.y.) which coincides with the Cretaceous-Tertiary boundary <K-T. boundary), the period of phenonenal nass extinctions on a Global scale. The Deccan Traps are now to be considered second only to Coluebia River basalts in respect of the wealth of inforuation we have, particularly with regard to stratigraphy and chenical characters. Though in general the lava flows are constituted nostly of the tholeiitic basalts, the uonotony is somewhat broken along its western fringe where acidic and alkaline differentiates, to include rhyolites and trachytes, are present as sporadic occurrences and in addition there also occur deep green, extremely vesicular and somewhat tuffaceous spilitic rocks at Bombay islands. These flood basalts, as mentioned in the previous chapter (Chapter I) bear numerous cavity minerals like zeolites, phyllosilicates, carbonates, sulphates, molybdates and a variety of silica minerals, which are no doubt a reflection of the chemistry, course of crystallisation, structure, mode of eruption, and the tectonics involved in giving rise to this immense volcanic province. In view of this, a more detailed account on these aspects as available today, mostly through literature, personal observations and personal communications is incorporated in the following pages, with a special reference to the western part, to provide support to the contensions and conclusions drawn in this thesis and also for better understanding of cavity minerals under the present study. The Deccan Volcanic Province, the Deccan Traps as known since their early studies fro» the times of Captain Dangerfield, 1824 (in Ghodke, 1978) and covering an area around 500,000 sq. kn as presently available in more or less continuous exposures is likely to have spread over much larger area. The most conservative estimate given by Krishnan (1980, 1982) for the spread of this immense volcanic province is about 1,500,000 sq. km. It was also a long held view that the lava flows were the products of fissure eruptions and the dykes intruding them represented feeders of eruption. However, Krishnan (1949), Wadia, (1949), and Auden (1949), pointed out that the dykes in many cases belong to a post- trappean hypabyssal phase as also shown by Agashe and Gupte (1971) that many of them are true hypabyssal inJections under cover and there is no direct evidence to suggest them to be feeders. In general, it is held that the individual lava flows of the flood basalt province could be traced over long distances. Choubey (1973) considers a lava flow in the north-eastern part of the province to stretch from Sagar to Ratni for about 180 km. Beane a l ., (1983), Bodas et al. (1985), Cox and Hawksworth (1985) have all, on the basis of geochemistry of the basalt flows, reached similar conclusions and correlated flow groups between Pune and Mahabaleshwar situated over a distance of 100 km or so. West (1959) has shown that a fairly uniform thickness is maintained by such lava flows. However, in western Maharashtra, Marathe ai . , (1981) on the basis of extensive field studies have recognised four groups and shown that the 11 lateral extent of the individual flows is United to 20-40 . They have further held that these flows are highly vesicular and asaygdaloidal and pinch out laterally. This character led then to believe that such lavas erupted through central pipes and vents that produced volcanic breccia and highly zeolitised and hydrothernally altered basalts. 2.1 FLOW CHARACTERISTICS : The Deccan Trap lava flows which are uostly basaltic in nature »ay be broadly classified into "conpound" and "siitple" as suggested by Walker (1969) following the original concept of Hichols (1936). It neans that the lava flows are divisible into flow units considered as cooling units separated by tine intervals varying from hours to nonths. The flows which cannot be so divided into snaller units are considered as sinple. On the basis of the study of Hawaiian flows Macdonald <1953, 1972) proposed a classification of basaltic lavas into 'pahoehoe', ' aa' and 'block' lavas, each having distinctive physical characters depending upon the viscosity of the exuptive material. Walker (1969), after visiting a number of localities covering the DVP, expressed that the compound flows occurring in the Deccan Traps are pahoehoe. Phadke and Sukhtankar (1971) have shown a preference to distinguish the compound flows around Pune as pahoehoe. Similar scheme of classification of the Deccan Trap lava flows has been adopted by the Geological Survey of India as a simplified field classification, highly useful during geological mapping (e.g. Ghodke, 1969, 1970, 1978; Deshmukh, 1975, 1976, 1986; Godbole, 1987). The compound flows are most 12 extensive in the western part and constitute the bulk of the exposed sequence of the flows amounting to alnost 80% of the thicViness of the lava pile in this region (Deehnukh, 1888). The siuple flows have been equated with the aa flows by the GSI officers and it is a common experience that the pahoehoe and the aa (compound and simple lava flows) often occur in alternating sequences and differential weathering and erosion have given rise to a step like appearance to the topography of the region, the reason for the name Deccan Traps (Trapos = steps or stairs). Block lavas, in its true sense are, however, not recorded in the Deccan Traps but it is observed that at times the aa flows display some of the characters of the block lavas similar to the Yakima basalt flows of USA which could not strictly be representative of any of the three types (Kshirsagar, 1982). Similarly, a gradation from pahoehoe to aa, providing mixed characteristics to some of the lava flows similar to Macdonald's (1972) observations regarding the Hawaiian lavas may also be observed in the western DVP ( e.g. Kshirsagar, 1982). The task of the field geologist is highly simplified on account of such division of the basaltic lava flows into "compound" and "simple" or more so in terms of the GSI as "pahoehoe" and "a a ". The thickness of a compound flow varies in the range of few metres to 200 metres (Walker, 1969; Deshmukh, 1988) as seen in the Aurangabad region and the individual flow units are of much smaller magnitude. The famous Ajantha and Ellora caves are carved out in compound/pahoehoe flow having a thickness of around 50 m or more. Walker records a much thicker compound flow measuring about 190 m in the ghat section about 13 50 km south of Chalisgaon. Another instance of a very thick compound flow is observed near Trinbak, neasuring at least 160 n in which as many as 31 flow units are encountered. The sisple flows have characteristically lesser thickness but could be traced over longer distances. The different flow units in an overlapping sequence constitute the compound flow and the individual flow units have highly varying thickness in the range as low as few cm to as high as 15 m. The number of such flow units in a compound flow also varies greatly as seen in Kalsubai section where 33 flow units are encountered in a single compound flow measuring a thickness of 185 m. There is a distinct pattern of disposition of these flow units. The lowermost units have smaller thickness and constitute a thin pile overlain by thicker units of 5-15 m and are further overlain by a sequence of thinner units. In a single flow this pattern is repeated several times. On account of this variation, many times it is convenient to group the smaller lava flows rather than marking them as separate flows, as has been followed by the Geological Survey of India during the extensive task of basalt flow mapping. The variation in thickness as well as areal extent of the compound flows is particularly remarkable in the Vaitarna Dam site area, around Lonavala, around Pune, Ajantha caves as well as the Sangamner ghat section along Pune-Hasik Road. Deshmukh (1988) observes that the most extensive development of the basalt flows, compound in nature, is in the western part of the Deccan Volcanic Province and constitute comparatively an older sequence in relation to the simple flows.
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