AAPG II/fertli/fumal Cu4ermc( d EYhibifum '94 AJ/g/l.lf21-24, 1994, KJ/ala Lumpur, Maltzy"iLl
The Paleogene basins of Sabah, East Malaysia
F. TONGKUL
Earth Science Department Universiti Kebangsaan Malaysia, Sabah Campus Locked Bag No. 62, 88996 Kota Kinabalu, Sabah, Malaysia
Abstract: The Paleogene basins of Sabah developed in two stages, represented by early and late Paleogene sediments, in association with NW-SE compressional deformation during the late Mesozoic and Middle Eocene. The earlier deformation produced a wide elongate basin trending NE-SW bordered by a continental block to the NW and an emergent oceanic basement to the SE. The basin became the depositional sites of shallow to deep water early Paleogene sediments. The later deformation divided the earlier basin into two parallel basins (Outer and Inner basins) also trending NE-SW. Both basins were independently filled by shallow to deep water late Paleogene sediments derived axially from the southwest and laterally from the northwest and southeast. These basins were finally closed during the early Miocene resulting in the Paleogene fold-thrust belt of Sabah.
INTRODUCTION Sea oceanic crust in the SE (Fig. 1). The sediments covers most of western, northern and central Sabah The Paleogene basins of Sabah here refers to while in eastern Sabah the sediments are not clearly the depositional sites of thick Paleogene sediments mapped out due to the presence of extensive melange forming the mountainous belt of Sabah. Unlike deposits (Fig. 2). The Paleogene sediments continue most of the younger basins, the configuration of the southward onland into Sarawak and NE Paleogene basins were not preserved but greatly Kalimantan (Hamilton, 1979; Hutchison, 1989) and modified by compressional tectonics. The Paleogene northeastward offshore into Palawan (Rangin, sediments are characterised by severe folding and 1989). Paleogene sediments trending NE-SW thrusting. In western and southwestern Sabah the underlie much of the Neogene basins offshore sediments were mostly deposited by turbidity northwest Sabah (Bol and Hoorn, 1980; Hinz et al., currents and mass flows, and a northeast 1989). The continuation eastward offshore Sabah depositional direction has been established is still uncertain but is also thoughf to underlie (Stauffer, 1967; Tongkul, 1987). The elongate basin most of the Neogene sediments here. so-formed has been, informally referred to as the Rajang Basin or Crocker basin (Hamilton, 1979; STRATIGRAPHY Tongkul, 1987; Rangin, 1989; Hutchison, 1989). Detailed sedimentological, paleontological and The stratigraphy of Sabah, based on present structural informations on the sediments are still age determinations, is at best a general one (Fig. lacking in parts of western, northern, eastern and 3). The Paleogene sediments rest unconformably central Sabah. Therefore the overall nature and on Mesozoic oceanic crusts and overlain extent of the Paleogene basin is still unknown: unconformably by Neogene melange, pyroclastic and This paper presents additional information on clastic deposits. The precise age determination of the Paleogene sediments and proposes a model on most of the Paleogene sediments is still problematic the development of the Paleogene basins. due to lack of good fossil indicators. Therefore the relationship between some formations is still REGIONAL GEOLOGICAL SETTING uncertain and the tendency to lump them together is understandable. This, however, is not helpful in The Paleogene sediments form part of the NW understanding the depositional history of the Borneo subduction complex of Haile (1973) and sediments, because it is clear that the sediments Hamilton (1979) accreted during the Late Tertiary. were not deposited together as indicated by common These accreted sediments are bounded by the rifted facies variations within the sediments. southern continental margin of China presently Based on age differences, the Paleogene occupied by the Reed and Dangerous Grounds sediments can be broadly grouped into early and carbonate platforms in the NW and the Celebes late Paleogene deposits. The early Paleogene
Ceo!. Soc. Malay.,ia, Bulletin 37, July 1995; pp. 301-308 c.v o I\)
f- 1050 1100~:;:I EmI§ PRE-TERTIARY E§fE§ CONTINENTAL CRUST
I:·:·:"::·:·' TERRANE ACCRETED 15 0 .. : ::. SINCE LATE CRET.
INDOCHINA ACCRETED OR c=J EXTENDED CRUST BELOW SEA LEVEL
10 :n CONTINENTAL MARGIN rTml dz G> WJJ OF SOUTH CHINA . A I C I r- I \ \ ~ OCEANIC CRUST SUNDA \ 50 '- SHELF \ ( SUBDUCTION ZONES '\) !f;~ FOLD BELT 1/ , Sources: Hamilto!", 1979; Taylor &. Hayes, I 1050 1983; Hmz et.al., 1989; Hmz et.aL, II 1991. ttJ ;:: "- ~ ~S· ~------~ 1...1 Figure 1. Regional geological setting of Sabah. '1 116' liS' liS' Quarternary Alluvium If Lineaments Neogene-Quart. Igneous if/ Strike-Slip Fault RocJSULU SEA Neogene Sediments / Paleo flow Late Paleogene Sediments --l ::I: Early Paleogene Sediments m SOUTH CHINA SEA -C l> Mesozoic Ophiolitic .-m 0 Basement G) 6 m z 6' m tD ~ Z rn 0 "TI en l> tD l> _::I: m l> ~ s:: l> S rn» s' s' CELEBES SEA
Sources : Wilford, 1967; Yin, 1986; Tongkul. 1990.
SARAWAK Lineaments and faults based on Landsat images and SAR imageries interpretations.
19'
Figure 2. Geological and structural map of Sabah. w ow . SOUTHWEST WEST & NORTH CENTRAL EAST SABAH SABAH SABAH SABAH
PLIOCENE ~ ~. ,:, •.A LITHOLOGY Z ... : : :. '.: Go'7:-' ~.. t)~~ ·Sk~ .•~ ~ .... " ...... "{:J:'.~ ...... L ~ ...... Sb~ ..... ~-~ ·······By~ "O Q • ...... 0 t-- • .... J. ... Ii" Mudstone ~Kp~:':K~-=:, ~Tk ..To Kg~ 0 •..• :;;..-·c _ ili MIOCENE M .•-: 4~~ ~ t-- -=- --Se-- --=- -iif.Tifi.:~;::";· ...... Z E - - - -- .: ...... ~-;.& Sandstone '~ -:-.. ~.:- -;." UL~ ...... "''''6::I::: •••• - -~Me: ...... !....!.~ PL <>'" OLIGOCENE :-:- Ks .. ~:.. Lb-'-'-' Conglomerate ~ :Tx-~WCr' 00 Z ..... -(' ..... " ~ L _ > ..... !::=>.~ LL TLB r--, .• Limestone 0 I- fuSCr:~"" BL EOCENE ?. ;~ TL 0 M PBL~"?~ Pyroclastics ~ I- :-n ~ E c; ~ECr~ z Melange G> ~ ;><; PALEOCENE KL :p" ....••..•. Cr Chert I LATE ~~ ~o Basalt ~~ EARLY UU Ultrabasic 111111111111111 I Metamorphic ~~ Cb I- FORMATIONS: Be-Belait, Me-Meligan, Se-Setap, Tx-Temburong, WCr-WestCrocker, SCr-South Crocker, NCr-North Crocker, ECr-East Crocker, By-Bongaya, Sb-South Banggi, Wr-Wariu, Kd-Kudat, Tr-Trusmadi, Um-Umas Umas, Kp-Kapilit, Tj-Tanjong, Kb-Kalabakan, Km-Kuamut, Ks-Kulapis, Lb-Labang, Sp-Sapulut, Cs-Chert-Spilite, Sk-Sandakan, Gn-Ganduman, Sb-Sebahat, Ay-Ayer, Gr-Garinono, Kg-Kalumpang, Tu-Tungku, Cb-Crystalline Basement LIMESTONES: lJL.U\u Lakutan, KL-Kalampunian, DL-Dampirit, SL-Suangpai, LWL-Liwagu, ML-Maringan, BPL-Batu Puteh, TLB-Telupid, BL-Banggi, LL-Lian, BRB-Bayayo, RLB-Rompun, PL-Punggul, PBL-Pun Batu, GL-Gomantong, LBB-Langusan, TL-Tingkayu, TLL Larei Larei. CONGLOMERATES: MC-Malubuk, SC-Sensiang; BC-Bidu-Bidu. SOURCES: Clennell, 1992; Jumit, 1992; Basir, 1991; Tating, 1991; Rangin et al., 1990; Tongku~ 1990; Lai, 1989: Basir & Se1varajah, 1988; James, 1984; Langai, 1983; Lasimbang, 1983; Leong, 1974; Newton-Smith, 1967; Collenetle, 1965 & 1958;Wilson & Wong, 1964;Wilson, 1960; Fitch, \958; Stephen, 1956.
Figure 3. Generalised stratigraphy of Sabah. THE PALEOGENE BASINS OF SABAH, EAST MALAYSIA 305 sediments ranges in age from Late Cretaceous to STRUCTURE Early Eocene and includes formations such as the Sapulut, Trusmadi and East Crocker. The The Paleogene sediments which are commonly sediments assigned to the upper parts of the Chert folded and thrust-faulted exibits complex structural Spilite Formation has also been included here. The trends as a result of several episodes of deformation late Paleogene sediments ranges in age from Middle (Fig. 2). The major structural trend is shown by Eocene to Early Miocene and includes formation the sharp bend from NE-SW to NW -SE near Kota like the Temburong, Meligan, South Crocker, West Belud. The exact timing of bending is uncertain, Crocker, North Crocker, Kudat, Kulapis and Labang. but has been interpreted to have occurred sometimes during the Early Miocene (Tongkul, 1990, 1991, SEDIMENTOLOGY 1994). The bending has been related to the change in opening direction of the South China Sea basin The early Paleogene sediments consists mostly from NE-SW to N-S during this time (Taylor and of interbedded sandstones and mudstones deposited Hayes, 1983). Prior to the Early Miocene in deep water environments. Local occurrences of deformation, the sediments were deformed and limestones (Fitch, 1958; Collenette, 1965) and uplifted. The exact timing of deformation is also conglomerates (Newton-Smith, 1967; Leong, 1974) uncertain but is interpreted to have occurred suggests shallow water environments. The overall sometimes during the Middle Eocene (Tan & Lamy, depositional direction of the sediments is unclear 1990). This is indicated by the presence of an due to the scarcity of paleoflow indicators. The unconformity between the early and late Paleogene East Crocker sediments were derived from the south sediments in southwest Sabah. The early Paleogene and SE (Khor, 1994; Cheing, 1994). The occurrence sediments also experienced more intense of conglomerate in the Sapulut Formation deformation - some showing refolded folds and (Collenette, 1965) indicates a local source towards low grade regional metamorphisms (Langai, 1983; the SE. The thickness of the sediments is still James, 1984; Khor, 1994; Chieng, 1994) compared uncertain due to its complex structure but is to the late Paleogene sediments. The widespread estimated to be not more than 2,000 metres based occurrence of Middle-Late Eocene limestone also on measured sections on the East Crocker suggests such uplift. Formation (Khor, 1994). The late Paleogene sediments also consist DEPOSITIONAL MODEL mostly of interbedded sandstones and mudstones deposited by turbidity currents and mass flow in a A depositional model is proposed based on the deep water environments (Wilson and Wong, 1964; stratigraphy, sedimentology and structure of the Tongkul, 1987). Evidence for shallow water includes Paleogene sediments. It appears that instead of the occurrences of limestone lenses within the being deposited wholly in a single basin, the sediments (Stephen, 1956; Collenette, 1958; Wilson, sediments were deposited in two stages on more 1960; Wilson and Wong, 1964; Collenette, 1965; than one basin. Wilford, 1967; Leong, 1974; Lasimbang, 1983; Yin, The deposition of the early Paleogene sediments 1985; Basir and Selvarajah, 1988; Lai, 1989; Rangin probably occurred in a large open basin. This basin et al., 1990; Basir, 1991; Tating, 1991; Jumit, 1992). trends approximately NE-SW due to the subduction The depositional direction varies from place to place. collision of an oceanic lithosphere in front of a In southwestern Sabah, the Temburong, Southwest rifted continental block of China with the Celebes Crocker and South Crocker sediments shows a Sea oceanic crust during the late Mesozoic (Fig. consistent paleoflow towards the north (Wilson and 4a). The NW and SE part of the basin was bounded Wong, 1964; Stauffer, 1967; Tongkul, 1987; Low, by the continental block and an emergent basement, 1992), whereas in northern Sabah, the Kudat and respectively. The emergent basement in SE Sabah North Crocker Formations show a general paleoflow allowed the development of shallow water to the southwest and southeast, respectively limestones. The NE-SW geometry of the basin is (Tongkul, 1994). The red Kulapis sediments were based on the assumption that the major structural derived mostly from the NW (Tong, 1993), while bending occurred much later. This large basin the Labang sediments were mostly derived from continues southward and northeastward into the SE (Lim, 1990). The thickness of the sediment Sarawak and Palawan, respectively. The elongate is also uncertain and appears to vary from place to geometry of the basin allowed sediments to fill place. Measured sections from the West Crocker axially from the SW and laterally from the NE and and Kulapis Formations show thickness of about SE from the continental block and emergent 600 metres (Tongkul, 1987; Low, 1992) and 1100 basement, respectively. The huge size of the basin metres (Tong, 1993), respectively. enabled the development of several depositional
July 1995 306 F.TONGKUL
Emergent NW Southern Margin East Crocker Trusmadi Sapulut Basement SE of China Fm. Fm. Fm. PaleOCener-__ ~~~c-______~ __~~~C~ele~b~e~S_S~e~a ~~~~~~~--~~--~~~~=-~--~----~~--~~~~~~~~~~ - - "-:",;-~- ---"'" ~~~ - ..;, -::....~--- ~~,~=",~- ... " -~-:::- ~~--- '.:~:.t:).. -- _:: _-~~.-.. "-~v:a" ~=~:~ -- ~__ ~~=- .:r-~ .. -~~':- ~ .d9__ ~ ... -:'·;.f,'f· v -lI::o-"::- ,_ .::.;J
+ + + Oceanic Crust (a) + + Continental Crust
Outer Inner ~..---- Baain------·-~ ---Basin--- Structural High + Middle Eocene
+++++-t- -=-- 1"+1"+ .... + (b) ++++++ T + T ..,. +
Meligan W. Crocker & & Carbonate Reef Kudat Temburong S. Crocker Kulapis Labang Carbonate Reef Build-up Fm. Fm. Fm. Fm. Fm. Build-up
+++++-t-+ (c) + + + + T
NW Sabah Carbonate Platform Trough Segama Early Hills Miocene
+ -t- + + (d) + + + + .... + .... +
o 100 200 aDo 400 600 KM L'___ ~' ___~' ___~' ___~'~ __~'
Figure 4. Depositional model of Paleogene sediments. See text for further explanation.
GeoL. Soc. MaLaYJia, BuL1.etin 5, THE PALEOGENE BASINS OF SABAH, EAST MALAYSIA 307 environments. FITCH, F.H., 1958. The geology and mineral resources in the The deposition of the late Paleogene sediments Sandakan area, North Borneo. Br. Borneo Geol. Suro. by contrast, occurred in two parallel basins, an Mem.9. Outer and Inner basins trending NE-SW separated HAILE, N.H., 1973. The recognition of former subduction zones in Southeast Asia. In: Tarling, D.H. and Runcorn, by a structural high. The basins developed as a S.K. (Eds.), Implications ofContinental Drift to Earth Science, result of continued NW-SE compression in this 2. London Acad. Press, 885-892. region causing southward subduction-imbrication HAMILTON, W., 1979. Tectonics ofthe Indonesian region. U.S. of the oceanic basement and overlying early Geol. Suro. Prof. Paper 1078. Paleogene sediments (Fig. 4b). The geometry ofthe HINZ, K, FRISCH, J., KEMPTER, E.H.K, MANAF MOHAMMAD, A., basin is also based on the assumption that the MEYER, J., MOHAMED, D., VOSBERG, H. AND WEBER, J., 1989. major structural bending in the Paleogene Thrust tectonics along the continental margin of Sabah, sediments occurred later. The structural high Northwest Borneo. Geologische Rundschau 78/3, 705- allowed the development of shallow water 730. HINZ, K, BLOCK, M., KUDRASS, H.R AND MEYER, H., 1991. limestones. The elongate geometry of the Outer Structural elements of the Sulu Sea, Philippines. and Inner basins enabled sediments to fill axially Geologische lahrbuch, 127,483-506. from the SW and laterally from NW and SE, HUTCHISON, C.S., 1989. Geological evolution of Southeast Asia. independently. The huge size of both basins also Oxford Monographs on Geology and Geophysics No. allowed the development of different internal 13. Clarendon Press, Oxford, 386. depositional environments (Fig. 4c). By the end of JAMES, D.M.D., (ED.), 1984. Thegeologyand hydrocarbon resources Oligocene both basins were nearly filled and ofNegara Brunei Darussalam. Brunei Museum and Brunei carbonate reefs developed widely. The basins were Shell Petroleum Co. finally closed during the early Miocene resulting in JUMIT, J., 1992. Geologi am kawasan Wu Sg. Lakutan, Beaufort, the Paleogene fold-thrust belt of Sabah (Fig. 4d). Sabah. BSc. thesis, Universiti Kebangsaan Malaysia (unpublished). Subsequent deformation caused the major bending KHOR, C.H., 1994. Geologi am kawasan Tambunan Timur, Sabah. of this fold-thrust belt to its present configuration. BSc. thesis, Universiti Kebangsaan Malaysia (unpublished) . ACKNOWLEDGEMENTS LAI, S.K, 1989. Geologi am kawasan baratdaya Pulau Banggi, Kudat, Sabah. BSc. thesis, Universiti Kebangsaan Malaysia This ongoing research is funded by grants from (unpublished). UKM since 1987. Much of the data were obtained LANGAI,S.,1983. Geologikawasan Baratlaut Semenanjung Kudat, by the author's final year students. The author is Sabah. BSc. thesis, Universiti Kebangsaan Malaysia grateful to Marcus Jopony for his constructive (unpublished). comments on the paper and to Jupili Selamat for LASIMBANG, A, 1983. Geologi kawasan Timurlaut Semenanjung Kudat, Sabah. BSc. thesis, Universiti Kebangsaan Malaysia preparing some of the figures. (unpublished). LEONG, KM., 1974. The geology and mineral resources of the REFERENCES Upper Segama Valley and Darvel Bay area, Sabah, Malaysia. Geol. Surv. Malaysia Mem. 4 (revised). BASIR JASIN AND SELVA RAJAH, M., 1988. Paleogene planktonic LIM, E.W., 1990. Geologi kawasan Timur Kota Kinabatangan, foraminifera from Pulau Kalampunian Kecil, Sabah. Sabah. BSc. thesis, Universiti Kebangsaan Malaysia Sains Malaysiana 17, 67-69. (unpublished) . BASIR JASIN, 1991. Some larger foraminifera and radiolaria Low, T.H., 1992. Geologi am kawasan Wu Sg. Menggalong, from Telupid olistostrome, Sabah. 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------~... -~-+.-.------Manuscript received 15 November 1994
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