The milestone begins in 2022 whereby IRC, UTP in collaboration with UTP Geoscience Department and UTP Lab Management Department makes a first move to compile twenty-four (24) rock samples obtained from various origins in Malaysia. We are proud to share Sedimentary Rock, Metamorphic Rock & Igneous Rock collected from Perak, Kedah, Perlis, Negeri Sembilan, Kelantan, Johor, and Sabah. The treasures of the earth composed of natural minerals and fossils hail from different ages or eras such as Paleozoic (540 – 251 million years ago), Mesozoic (250 – 67 million years ago), and Cenozoic (66 – 5.34 million years ago).
Major Rock Type: Sedimentary Rock
Lithology: Mudstone
Formation: Gemas Formation
Age: Middle to Late Triassic (247 - 228 million years ago)
Origin: Ayer Hitam, Johor
This is a mudstone, from Gemas Formation. It is a fine-grained sediments with high carbonaceous contents. High carbon (C) had resulted the dark colour appearance. It appears to be thinly laminated (parallel lines making such a fabric pattern on the rock).
This rock was deposited in a deeper water environment, under low-energy condition (less waves and currents activities) with existence of volcanic activity during the same time.
Gemas Formation consist of mainly argillaceous rocks interbedded with volcanics and arenaceous rocks in the Southeast Pahang - Negeri Sembilan - North Johore area. Apart from this mudstone, Gemas Formation also preserved shale, siltstone, rhyolitic tuff and lenses of chert and limestone.
The age of this rock is estimated to be at middle Triassic age (about 247-228 million years ago). Several fossils including ammonite were found in the rocks from Gemas Formation. However, the sample that we have in IRC Display does not show fossils to the naked eye.
Thickness of rocks within the Gemas Formation can reach up to 5,500 meters and sometime is grouped together with Semantan Formation.
Generally, mudstone is used for pottery making to produce high-quality clays, as bricks, tiles and natural cement.
References:
1. Baioumy, H., Lehmann, B., Salim, A. M. A., Al-Kahtany, K., & El-Sorogy, A. (2020). Geochemical characteristics of black shales from Triassic turbidites, Peninsular Malaysia: Implications for their origin and tectonic setting. Marine and Petroleum Geology, 113, 104137.
2. Sajid, Z., Ismail, M. S., & Hanif, T. (2020). Mineralogical and geochemical imprints to determine the provenance, depositional history and tectonic settings of Triassic turbidites in the Semanggol and Semantan Basins, Peninsular Malaysia. Journal of Asian Earth Sciences, 203, 104539.
3. Raj, J. K. (2020). Residual shear strength of shales from the Gemas Formation based on ring shear tests. Warta Geologi, 46(3), 179-185.
Major Rock Type: Sedimentary Rock
Lithology: Sandstone
Formation: Bukit Bauk Formation
Age: Upper Paleozoic – Lower Mesozoic (307–174 million years ago)
Origin: Rimba Bandar, Bukit Bauk, Terengganu
The sandstone sample from Bukit Bauk shows brownish –yellowish colour rock sample, showing high content of iron-oxide leaching in the rock.
This sandstone has fine to medium grained minerals, consist of mainly quartz and feldspar with other lithified sediments.
Fractures are common in this sandstone, similar to other rocks that are found in the area of Dungun-Kemaman. The fractures are associated with structural and tectonic deformation that affected the eastern part of Peninsula Malaysia.
The sandstone is found in the area nearby Hutan Rimba Bukit Bauk, Dungun, Terengganu.
References:
1.Gasim, M. B., Sahid, I. B., Rahim, S. A., & Toriman, E. (2010). Characteristics of history, morphology and landform of the Dungun area, Terengganu, Malaysia with special reference to Bukit Bauk. Asian Journal of Earth Science, 3, 213-221.
Rock Type: Sedimentary
Rock Formation: Chuping Limestone
Age: Early Permian – Late Triassic (200 - 300 million years ago)
Locality: Bukit Chuping, Beseri, Perlis
References:
1. Razak, Y. A., Sum, C. W., & Othman, J. (2003). Sinkholes in the Bukit Chuping area, Kangar, Perlis.
2. AZALAN, S. A. (2015). SEDIMENTOLOGY, STRATIGRAPHY AND DIAGENETIC HISTORY OF BUKIT CHONDONG-BUKIT TUNKU LEMBUBUKIT CHUPING, PERLIS.
3. Adenan, N. B., Ali, C. A., & Mohamed, K. R. (2017). Diagenetic History of the Chuping Limestone at Bukit Tungku Lembu, Perlis, Malaysia. Sains Malaysiana, 46(6), 887-895.
Major Rock Type: Sedimentary Rock
Lithology: Sandstone
Formation: Bukit Puteri
Age: Lower - Middle Cenozoic (66 - 7 million years ago)
Origin: Bukit Puteri, Jerteh Terengganu
This sandstone is part of the unconsolidated conglomerate succession in Bukit Puteri, Jerteh. The conglomerate succession is found in several outcrops at level 188 m in Bukit Puteri.
The conglomerate succession composed of gravel size rocks clasts in subrounded to rounded shape. Some of the clasts are made of this creamy orange sandstone.
The sandstone has medium to coarse grains. The surface of the sandstone is rough and papery texture.
The sandstone and the whole conglomerate succession in Bukit Puteri is believed to be pushed out from the subsurface of the Earth around Cenozoic , based on its location along Terengganu major fault zone, and bounded by the Intrusive Granite Range.
The area of Bukit Puteri is famous for its mysterious myths among the locals.
References
Kadir, A. A. (2000). Antara Mitos dan Neotektonik Bukit Putri, Terengganu (IN MALAY), Geological Society of Malaysia Annual Geological Conference, September 8-9, 2000, Pulau Pinang.
Major Rock Type: Metamorphic Rock
Lithology: Marble
Formation: Kinta Limestone
Age: Devonian-Carboniferous (420 - 300 million years ago)
Origin: Chemor, Perak
This is another type of Kinta Limestone. Different to the previous sample, the colour is lighter and creamy. There are variations in the rock sample with slight reddish lines visible on the surface.
The minerals composition in this light-coloured Kinta Limestone are calcite, dolomite and hematite. The calcite can be identified as bedded grey sections of the rock composed of mainly calcium carbonate (CaCO3).
Dolomitic sections of the rocks can be recognized through pure-cream colour. Dolomite is a am anhydrous carbonate mineral composed of calcium magnesium (CaMg(CO3)2 . It will exhibit nice tabular crystal under the microscope.
The red lines visible in this sample is made of hematite. Hematite is a common iron oxide compound consist of Fe2O3 . The original colour of the hematite is metallic grey but it can become rusty-red in earthy composition. The ancient people use rusty-red hematite to draw on the cave wall. We can see some of this pre-historic treasure in caves around Gua Tambun in Ipoh.
References:
1. Mohd Isha, N. S., Mohd Kusin, F., Ahmad Kamal, N. M., Syed Hasan, S. N. M., & Molahid, V. L. M. (2021). Geochemical and mineralogical assessment of sedimentary limestone mine waste and potential for mineral carbonation. Environmental Geochemistry and Health, 43(5), 2065-2080.
2. Pierson, B. (2009). The limestone hills of the Kinta Valley: a part of Malaysia’s geological heritage worth preserving. first break, 27(11).
3. Muhammad, R. F., & Komoo, I. (2003). Lanskap kars Lembah Kinta warisan kebangsaan yang perlu dipelihara (IN MALAY), The Kinta Valley karst landscape—A national heritage to be preserved.
Major Rock Type: Metamorphic
Lithology: Hornfels
Formation: Jerai Formation
Age: Cambrian - Lower Carboniferous (550 - 350 million years ago)
Origin: Southern Part of Gunung Jerai
This is a low grade metamorphic rock from Jerai Formation in Kedah.
The hornfels formed from contact metamorphism of sedimentary rocks, usually shale or sandstone, when they were exposed to high temperature.
This rock is having dark grey-brownish red colour and has been polished for this display, hence it looks very beautiful.
The mineralogy of this hornfels consist of biotite, hornblende, pyroxene, and quartz. All the minerals are only visible through thin section (Md Ghazali, 2016).
References:
1.Md Ghazali, Luqman Hakim. (2016). Petrology of the southeastern part of the Gunung Jerai. FYP Dissertaition, Petroleum Geoscience, Universiti Teknologi PETRONAS.
2.Jones, C. R. (1968). Lower Paleozoic rocks of Malay peninsula. AAPG Bulletin, 52(7), 1259-1278.
3.Baioumy, H., Ulfa, Y., Nawawi, M., Padmanabhan, E., & Anuar, M. N. A. (2016). Mineralogy and geochemistry of Palaeozoic black shales from Peninsular Malaysia: Implications for their origin and maturation. International Journal of Coal Geology, 165, 90-105.
Major Rock Type: Sedimentary Rock
Lithology: Sandstone
Formation: Kati Beds Sandstone
Age: Carboniferous - Permian (359 -252 million years ago)
The rough surface texture of the rock indicated the coarser grains present, which is commonly sand-sized grains. The rock is cut by reddish iron-rich veins.
The Kati formation (now Kati Beds) is typically comprised of lithology in details comprised of reddish brown to purplish carbonaceous shales, siltstone, mudstone and rare red sandstones with minor conglomerates and lenses of carbonaceous limestone.
The finer sediments are characteristically laminated and grey in color. Sedimentary structures observed include rhythmic bedding, rare, graded bedding, and flute casts (Wong, in prep.). The formation is correlated with the Kubang Pasu formation.
Rock Type: Sedimentary
Rock Formation: Kepis Formation
Age: Lower Permian (299 - 274 million years ago)
Locality: Kepis, Bahau, Negeri Sembilan
Kepis limestone are dark grey and often with bedding (rock layers). Their black colour is due to the presence of carbonaceous materials.
The rocks have been slightly metamorphosed and become brittle, which resulted in the intense fracturing of the rocks. The fractures include faults and veins.
Look among the boulders for fragments of gold-coloured minerals called pyrite within the quartz veins. Pyrite is also known as “fool’s gold”.
References:
1. Jasin, B., & Ali, C. A. (1997). Significance of Early Carboniferous Radiolaria from Langkap, Negeri Sembilan, Malaysia.
2. Mohamed, K. R. (1996). Stratigrafi Jalur Tengah Semenanjung Malaysia (IN MALAY), Stratigraphy of the Central Belt of Peninsular Malaysia.
3. Peng, K. H. (1990). STRATIGRAPHY OF THE “MAIN RANGE FOOTHILLS” AREA OF PENINSULAR MALAYSIA. Laporan Persidangan Geologi Tahunan Yang Ke..., Kertas Teknik, 128.
4. Foo, K. Y., 1983. The Palaeozoic sedimentary rocks of Peninsular Malaysia – stratigraphy and correlation. Proceeding of Workshop on Stratigraphic Correlation of Thailand and Malaysia, 1, p. 1-1
Major Rock Type: Iron Ore (Parent Rock- Sedimentary)
Lithology: Iron Ore
Formation: Chemor Formation
Age: Lower Devonian – Middle Permian (419-273 million years ago)
Origin: Perlop, Sg. Siput
This panel represents the iron rich mineral or iron-ore from the parent rock of the pink dolomite described earlier. The iron ore is quarried in the area of Sungai Siput, Perak for its usage to make steel and other industrial purposes.
This iron ore is believed to be occupying the shear zone in Kinta Valley. Shear zone was a zone where structural deformation was active in the past.
A pure iron-ore should be highly magnetized and can be useful to attracts metal elements.
References:
Major Rock Type: Sedimentary Rock
Lithology: Limestone (fractured and infilled by minerals)
Formation: Kinta Limestone
Age: Devonian-Carboniferous (420 - 300 million years ago)
Origin: Sungai Siput, Perak
This is another type of Kinta Limestone. Different to the previous sample, the colour is lighter and creamy. There are variations in the rock sample with slight reddish lines visible on the surface.
The minerals composition in this light-coloured Kinta Limestone are calcite, dolomite and hematite. The calcite can be identified as bedded grey sections of the rock composed of mainly calcium carbonate (CaCO3).
Dolomitic sections of the rocks can be recognized through pure-cream colour. Dolomite is a am anhydrous carbonate mineral composed of calcium magnesium (CaMg(CO3)2 . It will exhibit nice tabular crystal under the microscope.
The red lines visible in this sample is made of hematite. Hematite is a common iron oxide compound consist of Fe2O3 . The original colour of the hematite is metallic grey but it can become rusty-red in earthy composition. The ancient people use rusty-red hematite to draw on the cave wall. We can see some of this pre-historic treasure in caves around Gua Tambun in Ipoh.
References:
1. Mohd Isha, N. S., Mohd Kusin, F., Ahmad Kamal, N. M., Syed Hasan, S. N. M., & Molahid, V. L. M. (2021). Geochemical and mineralogical assessment of sedimentary limestone mine waste and potential for mineral carbonation. Environmental Geochemistry and Health, 43(5), 2065-2080.
2. Pierson, B. (2009). The limestone hills of the Kinta Valley: a part of Malaysia’s geological heritage worth preserving. first break, 27(11).
3. Muhammad, R. F., & Komoo, I. (2003). Lanskap kars Lembah Kinta warisan kebangsaan yang perlu dipelihara (IN MALAY), The Kinta Valley karst landscape - A national heritage to be preserved.
Major Rock Type: Sedimentary Rock
Lithology: Limestone
Formation: Kinta Limestone
Age: Devonian-Carboniferous (419 - 273 million years ago)
Origin: Sungai Siput, Perak
Limestone is a sedimentary rock which was deposited in a shallow marine. It composed principally of calcium carbonate, CaCO3 (calcite mineral). The mineral composition in this limestone is not clearly visible to the naked eyes. We will need to use microscope to recognize the mineral composition in this rock sample.
Commonly, the limestone is made of with pure calcite mineral. The calcite mineral is colourless. If there are impurities present in the limestone e.g. mud, carbon, the colour of the rock become grey or dark grey, which is showed in this dark/blacky limestone sample.
The black limestone of Kinta Valley is a beautiful rock because it is intercalating with fractures. The fractures are visible to the naked eyes, as they are now filled up by whitish calcite mineral. The fractures were created after the limestone rock was deposited during tectonic deformation.
Some of the limestone around Kinta Valley have been metamorphosed. The metamorphism of the is associated with the intrusion of the Main Range granite as it provides enough source of heat to change the limestone into marble. The process is known as contact metamorphism.
The Kinta Limestone forms part of the ‘Calcareous Series’ of Ingham and Bradford (1960). It is commonly used for construction, tabletop and landscaping.
References
1. Rastall, R. H. (1927). The Limestone of the Kinta Valley, Federated Malay States. Geological Magazine, 64(9), 410-432.
2. Zabidi, H., Termizi, M., Aliman, S., Ariffin, K. S., & Khalil, N. L. (2016). Geological structure and geomorphological aspects in Karstified susceptibility mapping of limestone formations. Procedia Chemistry, 19, 659-665.
3. Hui, P. X., Ramkumar, M., Nagarajan, R., Mathew, M. J., & Ng, T. F. (2021). Episodic dolomitization of Paleozoic limestones in the Kinta Valley, Malaysia: implications on porosity evolution and reservoir properties. Energy Geoscience, 2(4), 298-307.
Calcite veins in grey limestone. Big arrow indicated the compression direction resulted the fractures/veins, small arrow indicated the extension direction.
Major Rock Type: Metamorphic Rock
Lithology: Schist
Formation: Jerai Formation
Age: Cambrian (539 - 485 million years ago)
Origin: Titi Hayun, Yan, Kedah
This rock is called as a schist. It is a metamorphic rock, originated from sedimentary rock (parent rock), after being exposed to a moderate level of heat and pressure (metamorphism). It also underwent changes in the chemical composition. Commonly, the parent rocks (geological term: protoliths) are either shales or mudstone.
This Titi Hayun Schist is part of the lithofacies associated with Jerai Formation. Rocks found in Jerai Formation comprised of Quartz arenite with occasional felsdpar grit, quartz-mica shicst and phyllite with occasional amphibole and garnet-bearing schist.
The schist from this sample shows foliation. Foliated metamorphic rock made up of plate-shaped mineral grains that are large enough to see with an unaided eye. It usually forms on a continental side of a convergent plate boundary where sedimentary rocks were put in intense environment (moderate pressure and temperature), able to convert the clay minerals (in shales or mudstone) into platy metamorphic minerals such as muscovite, biotite, and chlorite. The platy minerals can also be graphite, talc or hornblende if the origin (parent rock) is from basalt.
To become schist, a shale or mudstone must be metamorphosed in steps through slate and then through phyllite. If the schist is metamorphosed further, it might become a granular rock known as gneiss.
Schist is a beautiful rock, strong and durable. We usually used shist as decorative rock for building houses and walls.
References:
1.Khoo, T. T., & Tan, B. K. (1983, September). Geological evolution of peninsular Malaysia. In Proceedings of the Workshop on Stratigraphic Correlation of Thailand and Malaysia (Vol. 1, pp. 253-290). Geol. Soc. Thailand and Geol. Soc. Malaysia Bangkok.
2. https://www.geoventuresolution.com.my/rocks-that-can-be-found-in-batu-hampar-and-titi-hayun-jerai-kedah/
Major Rock Type: Igneous Rock
Lithology: Biotite Granite
Granite province: Main Range Province
Age: Late Triassic (230 - 200 million years ago)
Origin: Tampin, Negeri Sembilan
This is a granitic rock, collected from Tampin, Negeri Sembilan. Granite is an igneous rock which showed its magma origin. The colour is light grey. Granite is composed of different minerals such as quartz, feldspar and mica biotite. The individual minerals can be recognized based on their colours, shapes and characteristics.
Quartz minerals in Tampin Granite is colourless and has no standard shapes. It’s chemical composition is SiO2. Quartz is one of the most abundant minerals on the Earth's crust. The minerals are highly resistant to physical and chemical weathering.
Feldspar minerals in Tampin Granite are white in colour and sometimes appeared in “rectangular” shape. Feldspar is a group of aluminosilicate minerals that contain calcium, sodium, or potassium.
Biotite of Tampin Granite has a dark brown colour and typical platy feature. Biotite is regarded as a mixture composed of variable proportions of four basic aluminosilicates of potassium, iron, magnesium, or aluminium.
The crystal sizes of the igneous rock can tell the cooling rate of the magma, i.e. slow cooling resulted coarse grains and fast cooling resulted fine grains. Thus, the coarse-grained texture in Tampin Granite (> 0.5cm of mineral size) is resulted from the slow crystallization of magma below the Earth's surface.
Granite is well known by public. It is the most common igneous rock found on the Earth's surface and granite is also often used to make many products such as countertops, floor tiles, paving stone, curbing, stair treads, building veneer, and cemetery monuments.
References:
1. Ghani, A. A., Searle, M., Robb, L., & Chung, S. L. (2013). Transitional IS type characteristic in the main range granite, Peninsular Malaysia. Journal of Asian Earth Sciences, 76, 225-240.
2. Seong, K. T. (1990). K-Ar dating of micas from granitoids in the Kuala Lumpur-Seremban area.
3. Tschang, H. L. (1962). Some geomorphological observations in the region of Tampin, southern Malaya. Zeitschrift für Geomorphologie, 6, 253-259.
Close-up view of the granite and indication of different types of minerals (Q: quartz, F: feldspar, B: biotite)
Major Rock Type: Igneous
Lithology: Granite
Formation: Kemahang Granite
Age: Triassic (251-201 million years ago)
Origin: Kampung Jedok, Tanah Merah
(Quarry Dimensi Timal Sdn. Bhd)
Kemahang granite was first described by MacDonald (1967). This igneous rock formation occupies the northwest of Kelantan state, close to the Thailand border.
Kemahang granite is greyish in colour, with traces of pale yellow-reddish spot due to the weathering. It is dominated with medium to coarse grain minerals.
The mineralogy of Kemahang granite consists of large feldspar phenocrysts, biotite and quartz. Phenocryst is a term referring to larger crystal of mineral that is very obvious and distinct from the groundmass.
The large feldspar phenocrysts are found to be lineated (arranged in lines). This lineation feature indicates that Kemahang granite had underwent intense tectonic deformation (shearing) in the western side of the formation.
Commonly, the sheared rock will went through low-grade of metamorphism and will be transform into metamorphic rock. However, based on physical evidence, there is no evidence of metamorphism preserved in Kemahang granite, hence it is still considered as an igneous rock. The evidence of metamorphism can be seen in Taku Schist, which in contact with Kemahang granite.
References:
1.MacDonald, S., (1967). Geology and mineral resources of north Kelantan and north Terengganu. District Memoir 10. Geological Survey West Malaysia, 202.p.
2.Heng, G. S., Hoe, T. G., & Hassan, W. F. W. (2006). Gold mineralization and zonation in the state of Kelantan.
3.Khoo, T. T., & Lim, S. P. (1983). Nature of the contact between the Taku Schists and adjacent rocks in the Manek Urai area, Kelantan and its implications.
Major Rock Type: Sedimentary Rock
Lithology: Sandstone
Formation: Tebak Formation
Age: Upper Jurassic to Lower Cretaceous (163 -100 million years ago)
Origin: Kluang, Johor
This is a quartz-rich sandstone. The high quartz content provided the light colour of the rock. Quartz is a mineral made of silica.
The rock was deposited in a terrestrial environment such as fluvial system and is part of Tebak Formation. Some of the classification refers it to Panti Sandstone.
Tebak Formation was introduced by Rajah S.S. (1968 unpublished) for a unit of predominantly arenaceous rocks in the central and southern part of the Gunung Blumut area in the southern Johore.
Although no fossils have been found in Tebak Formation in this area, an Early Cretaceous age is deduced on its assumed to be similar and correlated with the Panti Sandstone in the southern part of Peninsular Malaysia. The correlation is done based on the lithological content of arenaceous mineral (quartz arenite, quartz wacke, feldspathic arenite) with minor siltstone and grey - purple mudstone. In the real outcrop, thin coal seams are also present.
Not far from this area, plant fossils were found in Kahang Formation, indicate a Late Jurassic to Early Cretaceous age.
This rock is important in understanding the paleo-climate (climate in the past), which indicate warm and dry climate during the deposition time. We can use it to interpret the past and predict the future climate of our Earth.
References:
1. Said, U., & Ali, C. A. (2000). On the Palynomorph Assemblage from the Panti Sandstone, Kota Tinggi, Johor.
2. Tjia, H. D. (1996). Tectonics of deformed and undeformed Jurassic-Cretaceous strata of Peninsular Malaysia.
3. Shirlaw, J. N., Pakianathan, L. J., & Kumarasamy, J. A Review of the Variability of the Strength and Abrasivity of the Rocks of the Jurong Group and Tebak Formation.
Description:
References:
Kumar, S. C. (1980). Titanaugite from Bukit Kemuning, Kemaman, Trengganu. Warta Geologi, 1-5.
Ghani, A. A. (2005). Geochemical characteristics of S-and I-type granites: example from Peninsular Malaysia granites.