Mesozoic and Tertiary tectonics of Irian Jaya: evidence for non-rotation of Kepala Burung

Henage, Lyle F.

doi:10.29118/ipa.213.763.792

Cited by 5 publications

(6 citation statements)

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“…Mesozoic and Tertiary tectonics have developed the basin embayment. Some of them are Late Tertiary clockwise rotation, counterclockwise rotation, or no significant rotation of Bird Head due to the continuity of rift and collision related structural trends across Irian Jaya since Jurassic (Henage, 1993). To be objectives, a seismic sequence analysis reached out without any other information except seismic data.…”

Section: Results and Analysismentioning

confidence: 99%

Tertiary Sequence Stratigraphy of Bird Head Area, Eastern Indonesia

Alam

Setiadi

2019

Indonesian J. Geosci.

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A long depositional period of Papua limestone called Kais Formation, which is overlain by clastic sediments of Steenkool Formation, reflects an interesting stratigraphic architecture in the West Papua region. Using seismic stratigraphic method of five stacking patterns, forestepping, downstepping, upstepping, backstepping, and seismic facies (parallel, prograding clinoform, channel fill, mounded) have been observed. Chronostratigraphic reconstruction was completed to figure out the depositional units in space and time. This study reveals the lowstand deposit during Early to Middle Eocene (LST), transgressive-highstand carbonate deposit during Middle Eocene to Middle Oligocene, and transgressive-highstand silisiclastic (TST-HST) deposit during Middle Miocene-Late Pliocene.

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Section: Results and Analysismentioning

confidence: 99%

Tertiary Sequence Stratigraphy of Bird Head Area, Eastern Indonesia

Alam

Setiadi

2019

Indonesian J. Geosci.

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“…Several authors (e.g. Hamilton, 1979;Johnson a Jaques, 1980;Dow & Sukamto, 1984;Pigram and Panggabean, 1984;Pigram and Davies, 1987;Daly et al, 1991;Struckmeyer et al, 1990 and1993;Cloos et al, 2005) emphasized different tectonic processes. Thus, it would certainly give no quantitative description of geological evolution in eastern Indonesia in providing the basis for evaluating the geological knowledge.…”

Section: Discussionmentioning

confidence: 99%

Tectonostratigraphy of the Southern Part of Papua and Arafura Sea, Eastern Indonesia

Harahap

2012

Indonesian J. Geosci.

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DOI: 10.17014/ijog.v7i3.145Sedimentary history and stratigraphy of the Papua and Arafura Sea areas, eastern Indonesia, are gained from surface geological mapping combined with published data from oil companies. Development of some sedimentary units demonstrates that the tectonism have influenced sedimentation of such units comprising a succession of Phanerozoic rocks developing in a stable continental margin. The succession underlain by Cambrian-Silurian-Devonian metamorphic rocks consists of Tuaba, Kariem, Awitagoh, and Kemum Formation, and Modio Dolomite (Pre-Rift Phase). These rocks having been intruded by Late Permian-Middle Triassic granitoids and Carboniferous granite, are unconformably overlain by Late Carboniferous to Cretaceous siliciclastic-rich units comprising Aifam Group and Tipuma Formation (syn-Rift Phase) and Kembelangan Group (Mesozoic Passive Margin Post-Rift). The Aifam Group is separated by a regionally continuous boundary on its top contact from the Triassic-Early Jurassic Tipuma Formation, which filled the block-faulted rift valley subbasins of continentally deposited red beds in the breakup stage. Regionally, developed erosion surfaces of the breakup unconformity have separated these red beds from generally transgressive post-breakup deposits of the Jurassic to Cretaceous marine sediments of the Kembelangan Group. Beach to shallow marine-glauconitic sandstone and shale of the group pass upward into shelf mudstone. Relative sea level fall related to the tectonic stability of the area led to the development of Eocene to Late Miocene platform carbonates of the New Guinea Limestone Supergroup which occurred in the entire island of Papua and the southern of Arafura that overlie these non-carbonate units (Tertiary passive margin). It is separated from the siliciclastic-rich packages by the Tertiary - Pre-Tertiary boundary. The sea level fluctuation within the group was also recorded during the formation of thin, discontinuous sandstone beds/lenses of Sirga Formation and Adi Member of the Oligocene age (Convergence phase). Turbidite sediments of the Miocene Klasafet Formation was deposited in a deep marine environment at the same time as the eruption of magmatic arc (Compressional phase). The mainland area was exposed above sea level at Late Miocene to Pleistocene (Melanesian Orogeny) and terrigenous detritus deposition began to fill in the basin as molasses type deposits with a marine influence in part (Buru and Steenkool Formations).

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“…Ditinjau dari struktur geologi regionalnya, area studi di Cekungan Bintuni terletak pada tumbukan tepi Lempeng Benua Australia Utara dengan Lempeng Samudra Pasifik (Hamilton, 1979). Area Studi MT yang relatif terletak di bagian utara Lempeng Australia dikarakterisasi dengan sesar-sesar purba berarah U 300 T (Henage, 1993) seperti yang ditunjukkan pada Gambar 1. Lintasan MT sepanjang 20 km yang berarah timurlautbaratdaya yang tegak lurus dengan arah sesar-sesar tersebut.…”

Section: Geologi Regional Area Studiunclassified

“…Untuk mengetahui struktur secara regional, digunakan data gayaberat satelit GGMPlus (Gambar 4). Kotak berwarna merah merupakan area pengukuran MT yang o menunjukkan adanya struktur berarah relatif U 300 T. Data gayaberat satelit ini sekaligus mengkonfirmasi studi sebelumnya yang menyatakan keterdapatan struktur-struktur purba dengan arah yang sama (Henage, 1993). Kelurusan gayaberat yang dicirikan dengan garis berwarna hitam pada Gambar 4, juga mengkonfirmasi struktur geologi yang tersingkap di permukaan yang 10.400 -0.000034 Hz.…”

Section: Hasil Metode Gayaberat Ggmplusunclassified

Interpretasi Penyebaran Batuan Induk Pada Cekungan Bintuni, Papua Barat Berdasarkan Analisis Data Magnetotelurik dan Gayaberat

Wang

Rohiman²,

Marjiyono³

et al. 2022

JGSM.Geologi

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Integrasi data magnetotelurik (MT) dan gayaberat satelit digunakan untuk mendelineasi keberadaan batuan induk di bawah permukaan di Cekungan Bintuni. Data MT diperoleh dengan survei darat sebanyak 8 titik pengukuran yang membentang sepanjang 20 km berarah timurlaut-baratdaya. Pengolahan data MT berhasil meningkatkan kualitas data dari rentang 53,17 - 74,53 % ke rentang koherensi 78,57 - 91,12 %. Data MT dengan kualitas baik selanjutnya digunakan untuk melakukan pemodelan bawah permukaan. Data gayaberat diperoleh dari data GGMPlus yang memiliki resolusi spasial sebesar 200 m. Data berupa gravity disturbance kemudian diolah hingga memperoleh anomali Bouguer lengkap. Selanjutnya, anomali Bouguer lengkap ditapis untuk memperoleh sebaran anomali residual. Hasil dari metode gayaberat menunjukkan adanya klosur anomali tinggi dan rendah dengan arah baratlaut -tenggara yang diduga merupakan sumbu antiklin-sinklin di sekitar area yang tersesarkan geser mengiri berarah timurlaut - baratdaya. Geometri struktur geologi berupa antiklin dan sinkin tersebut dikonfirmasi oleh penampang vertikal MT yang sekaligus memetakan keberadaan puncak (top) anomali tahanan jenis rendah yang diperoleh di kedalaman 1.500 - 4.000 m di bawah permukaan. Anomali tahanan jenis rendah ini diduga merupakan respons keberadaan mature black shale Formasi Ainim yang berperan sebagai batuan induk di Cekungan Bintuni. Integrasi metode MT dan gayaberat ini dapat digunakan sebagai alternatif dalam studi regional pada Cekungan Sedimen.Katakunci: Cekungan Bintuni, gayaberat, GGMPlus, magnetotelurik, struktur geologi.Â

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Mesozoic and Tertiary tectonics of Irian Jaya: evidence for non-rotation of Kepala Burung

Cited by 5 publications

References 0 publications

Tertiary Sequence Stratigraphy of Bird Head Area, Eastern Indonesia

Tertiary Sequence Stratigraphy of Bird Head Area, Eastern Indonesia

Tectonostratigraphy of the Southern Part of Papua and Arafura Sea, Eastern Indonesia

Interpretasi Penyebaran Batuan Induk Pada Cekungan Bintuni, Papua Barat Berdasarkan Analisis Data Magnetotelurik dan Gayaberat

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