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Geology of the Magadi Area, Kenya % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % % %% % % % % % % % % % % % % % % % % % % % % % % % % %% % % % % % % % % % % %% % % % % % % % % % % % % % % % % % %% % % % % % % % % % % % % % % % % % % % % % % % % % % % % GEOLOGIC HISTORY % % % % % % % % % % % % % % % % % % % % % % % Legend % % % % % % % % % % % % % % % % %% % % % % % % % % % % % % % % % % % % % % % % % % HOLOCENE % % % % % % % % % Pleistocene Pleistocene: Gelasian % % % % % % % % %% %% %% % % % % %% % % Sediments % % % % %% % Evaporite Series (0-9 ka): trona with interbedded clays. The Magadi Soda Company at Lake Magadi % % % % %% %% % % % % % % % % % % % % % % % % % % % % % Pl-cv % currently mines the trona. % % Cinder cones Pl-let Leshuta Trachyte % % % % % % % % % % % % % % % % % % % % Holocene % % % % % Geology of the Magadi Area, Kenya % %% % % % % % % % % % % % % % % %% % %% % % %% % % % % % % % % % % PLEISTOCENE % % % Pl-kjb Kordjya Basalt % % % % % % % % % % % Nyokie % % %% % Trona % % % % % % % % % % % % High Magadi Beds (9-23.7 ka): yellow-brown silts over laminated clays with fish remains. Deposited during % % % % % % % % % % For area to North see: Geology of the Suswa Area, KGS Report 97; Digital version by A. Guth % % % % 36.5 °E % % % 36.0 °E % % % % % % % % % % % a period of higher lake levels in both lakes Natron and Magadi. % % % Pl-mt % % % % Mosiro Trachyte satellite lava % % % % % -1.5 ° % % % % % -1.5 ° % Alluvial fan % 0 % % % % % % % % 0 % % % % % % % Pl-tv % % % % 2 % % % % % % % % % 1 % % % % % % % % % % % % % Chert Series/Green Beds (40-96 ka): lacustrine chert and associated sediments up to 30 meters thick % % % Pl-et Ewaso Ngiro Trachyte % % % % satellite % % % Pl-mt % % % % Lacustrine Sediments % %% % Pl-mt % % % %% % above Oloronga beds. Cherts are typically surrounded by a green matrix of erionite tuffs and pyroclastic %% %% 0 % % 0 %% %% % %% 0 % 1 % silts, and may rise diapirically through the High Magadi Beds (Behr & Rhricht 2000, Behr 2002). %% % % 1 6 % % % 0 Pl-sb Singaraini Basalt % % ash flow 0 % 0 %% % 0 % 2 %% % Pleistocene % % 1 % % 1 % % % % 4 % % 0 % % 0 % % 0 Kedong Flood (100 ka): sand and fine gravel covering the Ol Tepesi plain. Evidence for a flood is given by % % 0 % 0 Pl-na welded tuffs %% %% % %% 0 1 Plio-Miocene % % % Pl-ml' High Magadi Pebble Beds % % % 0 % % % % % Baker & Mitchell (1976), and the source was likely the sudden emptying of Kedong Lake to the north. % % % Pl-et % %% %% % 0 % % 1 % % % % Mlt % % % % % Pl-kf These deposits are distinctive in satellite imagery, but can be quite thin. For example, south of the Magadi- % % % Pl-nv % % % Popn % % % % Ol Doinyo Nyokie Olorgesailie Nephelinite % % % % % % % % % % % % % % % % % % % Pl-ml High Magadi Beds % % % % % % % % Nairobi road, most exposures would be dominated by the lake beds of the Olorgesailie basin. % % % % % % % % % % 1 % % % % % % 6 % % % % %% % % 0 % % % % % % % % % Pl-kjb Pov % 0 % % % Olorgesailie % % % % % % % % % % Pleistocene: Calabrian % % % % % 0 Ol Tepesi Pl-c Magadi Green Beds % % % % % % % % % Orkaramatian Beds: white clayey lake sediments containing the remains of fish and gastropods. 0 % % % % ! % % % % % % % % 2 % % % % % % % %% % % % % % % % 1 Pl-okl %% % % % % %% % % % % % Deposition occurred near the Kirikiti fault, and sediments in the scarp rim suggest that the scarp was less % % % Mlt % % Pkb %% % % % % Pl-pt Kirikiti Basalt %% % % % % Magadi Trachyte %% % % % % %% % % % % % % Kedong Flood % % % % Pl-kf %% % % % % % % % than 20m high at the time of deposition (Crossley 1979). % % % % % % % % % % % %% % % %% %% % % % % % % % % % % % % % %% %% % % % % %% %% % % % % %% %% % % % % %% %% % % Pl-tv Mlt % % % % % Lengitoto Trachyte % % Tepesi Benmoreite % %% %% % % % 0 %% %% % % Pl-ogl % % % Oloronga Lake Beds % % Pl-ob % % % 0 %% % Oloronga Beds (300-800 ka): yellow water-lain tuffs are the remnants of a larger and fresher lake % % %% %% %% % 1 % % 4 0 % 0 % % % 0 % % % % % DDDD % % % % % 1 %% % % % % % 0 %% %% % % % % % 0 %% % % % % % %% % (Crossley 1979). About 45 m in outcrop, these sediments overlie the Magadi Trachytes, and contain chert, % %% %% % % 0 %% %% % % Pl-kt 1 %% % % % Mmn %% % % 1 1 Pl-tb DDDD %% % % Melanephelinites %% % % % %% % % 0 Tepesi Basalt %% % % % 8 % % % % % % 0 % % % % % Pl-ol % % 0 % % % % % Orkaramatian Lake Beds 0 % %% % % % % % % % kunkar limestone, and layers of carbonate boxwork (Baker 1958, Potts et al. 1988). % % % 0 % % % % DDDD % % % % % % % % % % % % % % % % % % %% %% % % % % % Ensonorua %% %% %% %% % % % %% % % 0 %% %% % % % ! %% % % % %% % % 0 % % %% % % % Pl-ob % % % Ol Keju Nero Basalt % 0 %% % % 0 % %% % 0 % % % % % % 0 %% % % 1 1 % %% %% %% % % % %% % Ol Doinyo Nyokie (0.66 - 1 Ma): trachytic ashes and obsidian erupted from a small cone. Chemical % %% % % Pleistocene: Calabrian %% %% %% % % Metamorphics %% %% %% %% %% %% %% %% %% %% %% % % 1 %% %% %% %% %% %% %% % compositions indicate Nyokie may be related to the Magadi trachytes (Baker 1975), and may also be the % % % 2 %% %% %% %% %% %% %% %% % % 0 Pl-kt %% % % North Kordjya Trachyte %% % % 0 % % % % % % % % % Pl-okl % % % Olorgesailie Lake Beds % % % % source for the Olorgesailie tephra (Deino & Potts 1990). % % % % % % % % % % % Xq Quartzites % % % % % % % %% % % % % %% % % % % %% % % % % % % % % %% % % % % %% %% % % %% %% %% % % % %% % % % %% % % Pl-tv % % % %% %% % % % %% %% % % % % % %% % Olorgesailie Lake Beds (0.2-1.2 Ma): diatomaceous, tuff and gravel beds of the Olorgesailie basin. The % % % %% % % % Xmg % % % % % % Muscovite schists % % % 1 % % % % % % % % % % % % 8 % % % Pl-cv % % % Volcanics % % % % % % Olorgesailie Formation has been divided into 14 Members (0.5-1Ma). The youngest lake deposits from 0 % % % % % % % % % % Pl-pt % % % % % % 0 % % % % % % % % % % 0 % % % % Mlt % % % % % % % % % % % 0 F % % % % % % % %% % 0.22 Ma (Deino & Potts 1990) were designated part of the Olkesiteti Formation (not distinguished here) by % % % % % % 2 %% % % Pl-cv % o % %% %% % % % % % % 1 %% % % % % r %% %% % % % %% %% % % % %% %% % % % % a %% % % %% %% % % % % Brooks et al. (2007). % % %% % % %% % 0 % % 0 % % 0 r % 80 % % %% % % % % % % e % % % % % % 0 % 0 % % % % % %% % % % %% % % % % %% % % 6 a % % % % 8 % % %% % % % %% % % % Pov 1 %% %% % % 1 % 2 % % % 0 1 % % 0 % % %%%%%%%%%%%%%%% ! % % % % % % t % % % % % % o % % % %% % % % % Pl-kjb % % % % faults-large City Road-major salt-ponds % 1 % % % % % % % % %% % % % % % % % % % % % 8 % E % % % % % % % Plateau/Magadi Trachyte (0.8-1.4 Ma): fine grained, peralkaline flood trachyte with a medium green to % % % % %% % % % % 0 % % %% % % % % a % 1 % % % % % % % % % 0 % %% % % % % s % % 0 %% % % % % % % % % % % % t % % % ! % brown-grey matrix, and feldspar phenocrysts up to 0.5cm. This prominent trachyte is found between Lake % 0 % % % % % % % % % % % % % % s % % 0 % % % faults-small Lake, ephemeral % % % % Town Road-minor % % % % % e % % % % % % % % % % % % % % e % % % % % Natron and Suswa, and is one of the several expansive "flood trachytes" that cover the rift floor. % % % % % % % % % % : % % % % % % % % 0 % % % % % % % % % % G % % % % % % % 0 % % % % % ! % % % % Mlt% % 0 % 6 e % % % % % % 0 % % % rivers % 8 % % % 1 Springs % % o % Village Road-track % % % % %% % % % % % % % % %% % % Pon l % % % % % o % % 0 % % % % % % %% % Ol Tepesi Basalts (1.4-1.65 Ma) and Benmoreites (1.42Ma): these two formations were distinguished by . % % % % % %% % % % g % 0 14 % % 0 % 0 % % % % 1 % % % % % % % % % % 8 y % %% % % % % % 7 % % %% %% % %% % % % % % % %% %% % % o % % % % % t %% % Baker & Mitchell (1976) from the Ol Keju Nero and Singaraini basalts based on age. The benmoreite flow % 1 % % % % 200m-contour % % % % Kamukuru % r % % % % % % % f % % rail Swamp % % % % 6 % % % % % %% % % ! 1 % % o 6 % % % % %% % % 0 t % % 0 % 0 % % % %% % % % % h %% % % % % Xq % p % % % % %% %% % 0 % % is at least 150m thick and features distinctive tabular and rhombic feldspar phenocrysts in a granular % % % % % % e %% %% %% % % % e % % % %% %% %% % % % % 1 % %% %% %% % % % %% % 0 % %% % % K % R % % 8 % %% % % % %% %% % % % % % % %% % 0 % % % 0 % PALEONTOLOGY % % % % a % % % % matrix. % % % % % % %% % % % S % 0 8 % % %% %% % % % j % % % % % i %% % 1 % % % % % % % a % G % % Pov %% % % % % % % % The lake beds at Olorgesailie host an impressive accumulation of stone hand axes, and Potts et al. (2004) announced the % % % 0 % % % %% % % %% %% % % d % % % %% % % %% % % % Pov 0 K %% % % % % % %% %% %% % % % %% % % % % 2 o % % % % % % , % %% %% % % % 1 % % %% % % discovery of a partial hominin skull from this locality. Early, Middle, and Later Stone Age artifacts are known from the Oloronga % % %% % a % % A 1 %% % % % %% % % % N. Kordjya Trachyte: (1.45-1.7 Ma): trachytes with abundant phenocrysts up to 2 cm in size, that were e GSU training ground 2 % r %% % r % % % % % % e % ! 0 beds, the Olkesiteti sediments (Olorgesailie Basin), and High Magadi beds respectively (Shipman et al. 1983, Potts and Deino %% % % % % A % % 0 a % % % 1 % % % % 0 2 previously mapped by Baker (1958) as "Orthophyre trachyte". These trachytes are intercalated with upper % 0 , s % 1 Pkb % % 0 l % % % % % % 0 1995, Barthelme et al. 2003). Pov K l % % % 6 % % i % % % % 0 % %% % % % % % G % 0 % %% % % % 1 H % %% % %% % % % members of the Kordjya basalt and have similar thickness and surface textures as the Ewaso Ngiro % 0 %% % % S %% %% % %% % % a % %% %% % t % %% %% % i % R %% %% %% % % STRUCTURE
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