BIBLIOGRAPHY OF THE GEOLOGY OF INDONESIA AND SURROUNDING AREAS Edition 7.0, July 2018 J.T. VAN GORSEL VIII. NEW GUINEA (incl. PNG) (( (Zwierzycki 1930, Map of Netherlands East Indies- Sheet XIII) www.vangorselslist.com VIII- NEW GUINEA/ WEST PAPUA and XI- PAPUA NEW GUINEA VIII- NEW GUINEA/ WEST PAPUA and XI- PAPUA NEW GUINEA ................................................................ 1 VIII 1-3. WEST PAPUA (WEST NEW GUINEA)............................................................................................. 21 VIII.1. New Guinea General and West Papua ............................................................................................ 21 VIII.2. Misool ........................................................................................................................................... 113 VIII.3. Arafura Shelf ................................................................................................................................. 121 IX 11-13. PAPUA NEW GUINEA ................................................................................................................. 128 IX.11. Papua New Guinea (East New Guinea main island) ....................................................................... 128 IX.12. Papua New Guinea (Bismarck Sea, Solomon Sea, Woodlark Basin) .............................................. 222 IX.13. Papua New Guinea (Gulf of Papua, Coral Sea).............................................................................. 256 This combined volume on New Guinea of Bibliography 7.0 contains 262 pages with >2010 references in six sub-chapters from both the Indonesian western part (West Papua: VIII.1- VIII.3) and the eastern part of New Guinea island (Papua New Guinea; IX.11- IX.13). The Indonesian, western part of New Guinea island is currently called West Papua; historically it has been known successively as Netherlands New Guinea, Irian Barat and Irian Jaya. The eastern part of the island is the independent nation of Papua New Guinea. Elegant recent overviews of the regional geology and tectonics of New Guinea are by Baldwin et al. (2012) and Davies (2012) (Figures VIII.1.1, VIII.1.2). Figure VIII.1.1. Main tectonic elements of the New Guinea region (Baldwin et al. 2012) Geologically, the main island of New Guinea is composed of: 1. The relatively undeformed Australian continental plate in the South, with Precambrian basement and relatively thin young sediment cover that is thickening into a foreland basin South of the Central Range; 2. Central Range fold-thrust belt of imbricated Mesozoic-Miocene sediments that were deposited along the Australian plate continental margin, and deformed during Miocene collision events with West Pacific arc systems; 3. Northern New Guinea 'Mobile Belt': a tectonically complex collage of Cenozoic Pacific oceanic arc systems, microcontinental blocks, ophiolites, metamorphics and Neogene sedimentary basins, the amalgamation of which was driven by the oblique convergence between the Pacific and Indo-Australian plates. 4. The 'Birds Head' in the NW, which does not readily fit with any of the above three tectonic domains. Its basement of imbricated Silurian-Devonian deep marine sediments intruded by Permian-Triassic granitoids is Bibliography of Indonesia Geology, Ed. 7.0 1 www.vangorselslist.com July 2018 much more similar to the Paleozic accretionary crust of PNG- East Australia than the Precambrian basement overlain by undeformed shallow marine Early Paleozoic of nearby West Papua. Figure VIII.1.2. Geological map of the New Guinea region (Davies 2012) Two different basement domains have been distinguished in the Australian Plate domain South of the Central Range, separated by an apparent continuation of the 'Tasman Line' of NE Australia (Figure VIII.1.1; see also Hill and Hall 2003): 1. Precambrian the West is part of the stable Australian craton, with Proterozoic metamorphics and granites, overlain by relatively undeformed Late Proterozoic and Paleozoic cover of shallow marine and non-marine intra-cratonic sediments; 2. Paleozoic: the eastern part (all in PNG) displays characteristics of the Eastern Australia/ Gondwana active margin, with highly deformed early Paleozoic marine sediments intruded by a belt of Permian- Triassic arc intrusives. (the 'Kemum Terrane' of the Birds Head of West Papua also displays these 'Tasmanide' Paleozoic active margin charactistics). The Central Range is composed mainly of complexly folded marine Jurassic- Early Miocene passive margin sediments. A long belt of ophiolites and associated metamorphic rocks along the northern margin of the Central Range foldbelt marks the suture between the Australian continental margin to the South and Pacific domain volcanic arc and ophiolite complexes in the North. Its emplacement marks the Early? Miocene collision of the Australian continent with an Oligo-Miocene age Philippine Sea volcanic arc. The Central Range, in both West Papua and Papua New Guinea, also contains a belt of Late Miocene- Recent dioritic intrusives and volcanics, many of which are associated with 'world-class' large porphyry gold-copper mineralizations. Some authors interpreted these intrusives as the result of South-directed subduction of Pacific Ocean (Philippine Sea) oceanic plate, after an older arc collision and subduction reversal. North of New Guinea island is the domain of the Westward-moving Pacific Ocean, which is composed of several tectonic sub-plates. Most of the oblique convergence with the North-moving Australia-New Guinea- plate is accommodated by subduction at the New Guinea Trench, but a significant component of transpressional deformation can be seen along several major E-W trending, left-lateral fault systems in northern half of New Guinea island (Koulali et al. 2014, etc.). Bibliography of Indonesia Geology, Ed. 7.0 2 www.vangorselslist.com July 2018 VIII.1. New Guinea General and West Papua (Irian Jaya) This sub-chapter VIII.1 of Bibliography 7.0 contains 768 refences on the geology of the Indonesian western part of New Guinea, as well as regional papers that cover the entire New Guinea region. The most comprehensive publication on the geology West Papua is still Visser and Hermes (1962), which summarizes the geological results of 30 years of petroleum exploration by the NNGPM (Shell-Caltex-Stanvac) consortium. Another book is by Dow et al. (2005), which is based on surface mapping work in the 1980's. Central Range The Central Range of West Papua formed as a result of collision of the Australian-New Guinea continental margin with a volcanic arc, along a North-dipping subduction zone. This probably took place before the Middle Miocene, as metamorphic-ophiolitic detritus from the Central Range is found in sandstones of the Middle Miocene Makats Formation North of the foldbelt (Visser and Hermes 1962). Figure VIII.1.3. Historic photo at ~4000m elevation of the ~4700m high, snow-covered peak of Mt Wilhelmina/ Trikora (Hubrecht, Third South New Guinea Expedition 1912/1913). Showing a ridge (Upper Cretaceous?) bedded sandstone overlain by massive Cenozoic New Guinea Limestone. The northern margin of this Central Range collision zone is a belt of obductucted ophiolites, that is underlain by a metamorphic sole that represents metamorphosed Jurasssic-Cretaceous deep marine distal continental margin clastics. Bibliography of Indonesia Geology, Ed. 7.0 3 www.vangorselslist.com July 2018 Figure VIII.1.4. N-S x-section of W (highest) part of the Central Range, showing peaks up to 5000m elevation composed of folded Eocene-Oligocene New Guinea Limestone, and the large exposed Ertsberg ('copper mountain') porphyry copper deposit at about 4000m. The lower areas are composed of Paleozoic- Mesozoic clastics and carbonates (Dozy, 1939). A second phase of uplift in the Late Pliocene-Pleistocene is apparent from the presence of outcrops of Late Pliocene dioritic intrusions, that crystallized at depth of at least a few kilometers, and are now exposed at altitudes of 4000m. Several of these intrusives are associated with world-class porphyry copper-gold mineralizations (Ertsberg, Grasberg, etc.). This uplift phase can be ascribed to slab breakoff/ collisional delamination after the underthusted Australian continental margin jammed the North-dipping subduction zone (Cloos et al. 2005). Birds Head paleo-position The Birds Head may well be a displaced terrane that was removed from a different part of the Australian- New Guinea margin. Today the Birds Head of West Papua moves as an independent microplate relative to the main body of New Guinea, in a SW direction at ~75-80 mm/year, which is twice as fast as any other continental block (GPS measurements in Stevens et al. 2002). Yet, many plate reconstruction models show the Birds Head as being more or less in the same relative position as today since the Mesozoic (Hall, etc.). Figure VIII.1.5. Present-day GPS motions show Birds Head as part of a separate plate (BHED) that is very rapidly moving to the WSW relative to South New Guinea- North Australia (Tikku 2008). Bibliography of Indonesia Geology, Ed. 7.0 4 www.vangorselslist.com July 2018 An alternative model proposed for the Birds Head is a paleo-position closer to the PNG side of New Guinea or NE Australia (Queensland) until Cretaceous time, when it separated during the opening of the Coral Sea (Pigram and Panggabean 1984, Struckmeyer et al. 1993, 1995, Davies 2012). This model was largely driven by the nature of the Early Paleozoic Kemum Formation basement of the Birds Head, which has a clear 'active