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All Journal Geological Engineering E-Journal IJOG : Indonesian Journal on Geoscience Jurnal Geologi dan Sumberdaya Mineral Scientific Contribution Oil and Gas Lembaran Publikasi Minyak dan Gas Bumi
Panuju Panuju
PPPTMBG Lemigas
Chemical Engineering, Chemistry & Bioengineering Earth & Planetary Sciences Education Energy Engineering Environmental Science

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STUDI SIKUENSTRATIGRAFI BERDASARKAN HASIL ANALISIS DATA PALINOLOGI PADA SUMUR Y, CEKUNGAN SUMATERA SELATAN Ramadhan, Rizki; Nugroho, Hadi; Aribowo, Yoga; Panuju, Panuju
Geological Engineering E-Journal Vol 5, No 1 (2013): Volume 5, Nomor 1, Tahun 2013
Publisher : Geological Engineering E-Journal

Show Abstract | Download Original | Original Source | Check in Google Scholar | Full PDF (1034.234 KB)

Abstract

Palynology is a study of biostratigraphy for determining relative age and depositional environment basedon the abundance of palynomorf. Palynology study develompent in Indonesia is still could be more increasedalong with more oil and gas exploration moved to transitional environtment.Study of palynology in stratigraphy is aiming to determine relative age and depositional environment.Besides, palynology could also determine sequence stratigraphy in a large scale of study based on palynomorfpercentage. The study of sequence stratigraphy based on palynomorf percentage has been done in Well-Y, SouthSumatra basin.The method of this research is descriptive method through the microscopic observation on sample 1 - 14from 1400 m depth Y-Well’s cutting and quantitative method calculation and analysis method from thisobservation and calcuation could determine the percentage of each palynomorf. This percentage lead to a trendthen interpretated into several sequencestratigraphy.From this observation, it can be determined characteristic zone of this well. The characteristic zone ofpalynology in this well is divided into 3 zones of palynology; Proxapertites operculatus Zone, Flocshuetziameridionalis Zone, and Stenoclaeniidites papuanus Zone. Each zone shows the characteristic of age fromEocene to Pliocene and also depositional environment from delta plain to pro delta. From palynomorfpercentage trend, we may also see the pattern of sequece stratigraphy works in this depth. The percentage trendshows the time whether sea level fall at the minimum percentage of palynomorf and sea level rise at themaximum percentage of palynomorf. The trend shows the sequence with sequence boundary lying in the startand the end of the sequence and also transgressive surface indicates the sea level start rise. Overall, this wellhas 5 sequences based on this trend; sequence a, sequence b, sequence c, sequence d, and sequence e and all thesequences are bordered by sequence boundary.
Nannoplankton Assemblage Succession Throughout Cretaceous/ Tertiary Boundary in the “P” Well Section, Santos Basin, Brazil Panuju, Panuju
Indonesian Journal on Geoscience Vol 6, No 1 (2011)
Publisher : Geological Agency

Show Abstract | Download Original | Original Source | Check in Google Scholar | Full PDF (1087.871 KB) | DOI: 10.17014/ijog.v6i1.115

Abstract

DOI: 10.17014/ijog.v6i1.115The massive change in calcareous nannoplankton assemblages throughout Cretaceous/Tertiary (K/T) boundary (65.5 M.a.) has been illustrated by several authors. The diverse and abundant assemblage disappears suddenly above the Cretaceous/Tertiary boundary. This event is related to the most dramatic environmental changes in the Earths history due to the catastrophic events, those are meteorite impact (Chicxulub) and supervolcano eruption (Deccan) occurring at the end of Cretaceous. The succeeding age was a time of rapid evolution of nannoplankton during Paleocene. A quantitative method analysis of nannoplankton throughout Maastrichtian to Paleocene of “P” well section, Santos Basin, Brazil, indicated that the nannoplankton assemblages abruptly decrease in diversity and abundance and mostly change in species composition. The various complex shapes of species at Maastrichtian also underwent changing to simple plain shapes and small at Paleocene. The sedimentary section ranges from the top of zone CC23 (Coccolith Cretaceous 23) to NP9 (Nannoplankton Paleogen 9). It is bounded by the Last Occurrence (LO) of Tranolithus pachelosus at the base and Fasciculithus tympaniformis at the top. The biostratigraphic discontinuity characterized by the absence of zone CC26 to NP4 is an indicator for the presence of an unconformity at K/T boundary within analyzed section. The Cretaceous nannoplankton assemblages are dominated by Genera Watznaueria, Micula, Arkhangelskiella, Cribrosphaerella, Eiffellithus, Predicosphaera, and Retecapsa, whilst the Paleocene assemblages are dominated by Genera Toweius, Ericsonia, and Coccolithus. Survivor Cretaceous species recovered into Tertiary sediments consist of Braarudosphaera bigelowii, Biscutum melaniae, Neocrepidolithus neocrassus, Placozygus sigmoides, Cyclagelosaphaera reinhardtii, Markalius inversus, and Scapolithus fossilis.
Perkembangan Fasies Sedimen Formasi Mamberamo Berumur Miosen Akhir-Pliosen di Cekungan Papua Utara Mamengko, David Victor; B.Sendjadja, Yoga; Mulyana, Budi; Panggabean, Hermes; Haryanto, Iyan; Lelono, Eko Budi; Musu, Juwita Trivianty; Panuju, Panuju
Jurnal Geologi dan Sumberdaya Mineral Vol 20, No 1 (2019): Jurnal Geologi dan Sumberdaya Mineral
Publisher : Pusat Survei Geologi

Show Abstract | Download Original | Original Source | Check in Google Scholar | Full PDF (310.459 KB) | DOI: 10.33332/jgsm.geologi.20.1.37-47

Abstract

North Papua Basin is a fore arc basin located in northern coastal of Papua Island. This basin filled by Middle-Upper Miocene turbidite sediment and overlied by Upper Miocene – Quarternary clastic sediment. Upper Miocene – Quaternary clastic sediments (Mamberamo Formation) composed by interbedding conglomerate, sandstone and shale as molasses deposit. A detailed stratigraphic study was performed to identify facies and its association of the Mamberamo Formation to that give a new perspective on the characteristics and development of facies succession of Lower Mamberamo Formation. Result  shows that the Lower Mamberamo Formation consists of three facies: A) cross bedding sandstone (subtidal), B) heterolothic silty shale (intra-tidal), C) carbonaceous shale (supra-tidal) deposited on Late Miocen to Plio-Pleistocene during centra range orogeny (syn-orogeny) as molasses deposits.Keywords: Fore arc basin, North Papua Basin, Mamberamo Formation, molasse deposits.
HYDROCARBON SHALE POTENTIAL IN TALANG AKAR AND LAHAT FORMATIONS ON SOUTH AND CENTRAL PALEMBANG SUB BASIN Julikah, Julikah; Sriwidjaya, Sriwidjaya; Hadimuljono, Jonathan Setyoko; Panuju, Panuju
Scientific Contributions Oil and Gas Vol 38, No 3 (2015)
Publisher : PPPTMGB "LEMIGAS"

Show Abstract | Download Original | Original Source | Check in Google Scholar | DOI: 10.29017/SCOG.38.3.549

Abstract

South and Central Palembang Sub - basin over Talang Akar (TAF) and the Lemat/Lahat Formations (LEF/LAF) has shale hydrocarbons (HC shale) which are considerably promising. Seismic interpretation results shows potential HC shale scattered in several areas around the Rukam-1, Kemang-1, Lion-1 and Tepus-1 wells. Generally, thermal modeling results indicates early maturity of oil on the value of Ro = 0.6% at about 2000 m depth (h), the formation of oil on the value Ro = (0.7-0.9)% at between (2200 £ h 3100) m depth and formation of gas at Ro values between (0.9-1.2)% at a depth between (3100-3500)m. Talang Akar and Lahat/Lemat Formations have a shallow marine depositional environment with Type II/III kerogen and lacustrine with Type III kerogen. Based on advanced seismic data processing (a method of seismic attributes and spectral decomposition) these areas are expected to have a TOC2% value that qualifies as shale HC. The assessment (P-50) of potential non-conventional oil and gas resources at Talang Akar and Lahat/Lemat Formations is estimated to be fairly large (up to 4200 MMBOE).
ANALISIS SIKUENSTRATIGRAFI UNTUK IDENTIFIKASI KOMPARTEMENTALISASI RESERVOIR KARBONAT FORMASI NGIMBANG BLOK SUCI, CEKUNGAN JAWA TIMUR UTARA (Sequence Stratigraphic Analysis for Identification of Carbonate Reservoir Compatementalization of Ngimbang Formation in Suci Block, North East Java Basin) Panuju, Panuju; Rahmat, Ginanjar; Priyantoro, Agus; Wijaksono, Egie; Wicaksono, Bambang
Lembaran publikasi minyak dan gas bumi Vol 51, No 3 (2017)
Publisher : PPPTMGB "LEMIGAS"

Show Abstract | Download Original | Original Source | Check in Google Scholar | Full PDF (1267.638 KB) | DOI: 10.29017/LPMGB.51.3.26

Abstract

Analisis sikuenstratigrafi telah dilakukan pada penampang sedimen Formasi Ngimbang di Blok Suci, Cekungan Jawa Timur Utara. Analisis ini dilakukan dengan tujuan untuk mengetahui suksesi vertikal dan perubahan fasies secara lateral dari unit sikuen reservoir karbonat pada Formasi tersebut sehingga kompartementalisasi fasies dari reservoir karbonat dapat dipahami secara rinci. Data yang digunakan dalam penelitian ini meliputi tiga well logs, biostratigrafi, lingkungan pengendapan dan petrografi dari sumur SUCI-1, SUCI-2 dan KMI-1 yang didukung penampang seismik. Penelitian ini dilakukan dengan mengintegrasikan semua data G G dalam kerangka kronostratigrafi dan model pengendapan karbonat sehingga kompartementalisasi yang mengontrol konektifitas dan sifat fisik unit-unit reservoir karbonat dapat dipahami dengan baik. Hasil analisis menunjukkan bahwa reservoir karbonat Formasi Ngimbang di Blok Suci diendapkan selama Eosen Akhir sampai Oligosen Awal pada lingkungan neritik pinggir sampai batial atas. Secara kronostratigrafi, penampang karbonat Formasi Ngimbang dapat dibagi ke dalam tiga unit sikuen yang dipisahkan oleh bidang keidakselarasan, yaitu unit facies karbonat platform berumur Eosen Akhir di sekitar lokasi sumur SUCI-2, unit fasies karbonat platform berumur Oligosen Awal bagian bawah di sekitar lokasi sumur KMI-1 dan SUCI-2 dan unit fasies core reef berumur Oligosen Awal bagian atas di lokasi sekitar sumur SUCI-1. Hasil analisis tersebut dapat digunakan untuk menjelaskan fenomena akumulasi gas yang hanya dijumpai pada lokasi sumur SUCI-1, dan hanya gas show dan oil trace yang terobservasi di sumur SUCI-2, serta indikasi hidrokarbon yang sama sekali tidak ditemukan pada sumur KMI-1. Hal tersebut terjadi karena reservoir karbonat fasies core reef berumur Oligosen Awal hanya dijumpai pada lokasi sumur SUCI-1 dan tidak menerus ke lokasi Sumur SUCI-2 dan KMI-1. Analisis kompartementalisasi ini akan dapat meningkatkan rasio keberhasilan perusahaan-perusahaan migas yang melakukan pemboran dengan target batuan reservoir berupa batuan karbonat.Sequence stratigraphic analysis has been conducted on the sedimentary succession of Ngimbang Formation in Suci Block, North East Java Basin. This analysis is performed to know the genetic relationship and lateral facies change of carbonate reservoir of the formation thus facies compartmentalization of this carbonate reservoir can be understood. The data used in this study include 3 well logs, biostratigraphy, depositional environment and petrography reports of the SUCI-1, SUCI-2 and KMI-1, supported by seismik sections. This study was conducted by integrating all G G data within Chronostratigraphy framework and carbonate deposition model thus compartmentalization controlling connectivities and physical properties among carbonate reservoir units can be well understood. Result of the analysis indicates that Ngimbang carbonate reservoirs in the SUCI Block were deposited during Late Eocene to Early Oligocene in the inner neritic to upper bathyal environments. The depositional setting of the sequences varies from shallow in the west (KMI-1) to become deeper in the east (SUCI- 2). Chronostratigraphy of the Ngimbang carbonate sequences shows three separated sequence units which include Late Eocene carbonate platform facies unit placing around the SUCI-2 well, the lower part of Early Oligocene to Eocene Carbonate platform facies unit at around both KMI-1 and SUCI-2 wells and the upper part of Early Oligocene core reef facies unit at around SUCI-1 well. All would be explaining how the gas accumulation does only occur in the SUCI-1 well, gas show and oil trace observed in SUCI-2 well, but no hydrocarbon indication found in the KMI-1 well. It is caused by a limited development of Early Oligocene core reef facies at SUCI-1 well location and not continuous to the location of SUCI-2 and KMI-1 wells. This compartmentalization analysis will increase the success ratio of oil and gas companies that drill with the target of carbonate reservoir rock.
The New Approach For Zonal Subdivision Of Pliocene - Pleistocene Nannoplankton Biostratigraphy In Waipoga-Waropen Basin, Papua Panuju, Panuju
Scientific Contributions Oil and Gas Vol 32, No 2 (2009)
Publisher : PPPTMGB "LEMIGAS"

Show Abstract | Download Original | Original Source | Check in Google Scholar | DOI: 10.29017/SCOG.32.2.844

Abstract

Waipoga-Waropen Basin is placed in northern part of Papua on the island of New  Guinea. The gas discoveries had been made since 1958 in this basin, however, no economic value of reserves lead to the not producing basin state until this time. The main problem in Waipoga-Waropen Basin is great thickness of Pleistocene sedimentary layers (until 7500m) as product of turbidite system (Wold Barret, 2000). This makes difficulty in well section correlation based on the conventional biostratigraphy since individual layers within that section is being small part of biozone. Many reworked nannoplankton as implication of turbidite deposit are also being complicated aspect in biostratigraphic analysis. The Pleistocene ranges from 1.806 m.a. to 11.550 k.a. It was the most recent episode of global cooling or ice age took place. In nannoplankton biostratigraphy, this age is characterized by the extinction of Discoaster brouweri (Discoaster group) at the bottom and the first occurrence of Emiliania huxleyi at the top. The quatitative nannoplankton investigation of “T” well has been done, and there is evident that its sedimentary section gives the excellent nannoplankton assemblages to subdivide Pleistocene age sediments of Waipoga-Waropen Basin (Zone NN19) into 9 subzones. Biomarkers from the bottom to the top consist of: LO of Discoaster brouweri, FO of Gephyrocapsa caribbeanica, FO of Gephyrocapsa oceanica, LO of Cacidiscus macintyre , LO of Helicosphaera sellii, FO of Reticulofenestra asanoi, FO of Gephyrocapsa parallela, LO of Reticulofenestra asanoi, FO of Helicosphaera inversa and LO of Pseudoemiliania lacunosa. The sediments belong to zone NN 20 that placed in the uppermost part of Pleistocene were not analysed.
Revised Zonal Subdivision Of The Late Miocene Nannoplankton Biostratigraphy For Kutei Basin Panuju, Panuju
Scientific Contributions Oil and Gas Vol 32, No 3 (2009)
Publisher : PPPTMGB "LEMIGAS"

Show Abstract | Download Original | Original Source | Check in Google Scholar | DOI: 10.29017/SCOG.32.3.849

Abstract

Lithological complexity and intense hydrocarbon exploration with the objective of Late Miocene sediments in Kutei Basin has provided the impetus for more refined Late Miocene nannoplankton zonation than the standard global schemes of Martini (1971). Investigation to the quantitative nannoplankton analysis results in Kutei Basin has been done, and there is evident that the deltaic sediments of this basin give an excellent nannoplankton assemblage dataset to refine the Late Miocene biostratigraphy. Biostratigraphically, Late Miocene ranges from the middle part of zone NN9 to the middle part of zone NN12 of Martini zonation (1971). Zone NN11 is the most crucial zone to be refined since this zone has long time interval (more than 2m.a.). In this paper, this zone can be subdivided into 7 subzones (NN11a-NN11g) based on relatively permanent occurrences of 6 biomarkers. They are from the base to the top, as follow: FO Discoaster quinqueramus, LO. Minilitha convalis, LO Discoaster bergenii, FO Amaurolithus primus, FO Reticulofenestra rotaria, LO, Discoaster berggrenii, LO. Reticulofenestra rotaria and LO Discoaster quinqueramus. In spite of zone NN9, NN10 and NN12 which have relatively short stratigraphic ranges, each zone can also be subdivided into 2 subzones. The base and the top of zone NN9 is indicated respectively by the FO and LO Discoaster hamatus. It can be subdivided by the FO Discoaster prepentaradiatus into subzone NN9a and NN9b. Zone NN10 is marked by the LO Discoaster hamatus at the base and FO Discoaster quinqueramus at the top. It can be subdivided into subzones NN10a and NN10b by the LO Discoaster bollii. Zone NN12 is characterized by the LO Discoaster quinqueramus at the base and the FO Ceratolithus rugosus at the top. This zone can be subdivided into subzone NN12a and NN12b by the LO Helicosphaera intermedia.
Co-Authors Agus Priyantoro Ali Djamhuri B.Sendjadja, Yoga David Victor Mamengko Eko Budi Lelono, Eko Budi Hadi Nugroho Hadimuljono, Jonathan Setyoko Hermes Panggabean Iyan Haryanto, Iyan Julikah, Julikah Musu, Juwita Trivianty Rahmat, Ginanjar Rahmat, Ginanjar Rizki Ramadhan Sriwidjaya, Sriwidjaya WICAKSONO, BAMBANG Wicaksono, Bambang Wijaksono, Egie Wijaksono, Egie Yoga Aribowo