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Permo-Carboniferous glacial Permodeposits of the Southern Huqf Alan Heward and Omar Al Ja’aidi 6-9 January 2005
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24th IAS MEETING OF SEDIMENTOLOGY IAS 2005 SCENIC SEDIMENTOLOGY Muscat Oman 10-13 January
F8 – Permo-Carboniferous glacial deposits of the southern Huqf, Oman. Leaders: Alan Heward (Petroleum Development Oman) and Omar Al Ja’aidi (Carbonate Centre, Sultan Qaboos University. This fieldtrip will examine glacial pavements and deposits of the Al Khlata Fm, and shallowmarine and continental deposits of the overlying Gharif Fm. Al Khlata and Gharif sandstones form important reservoirs for oil in the South Oman and Ghaba Salt Basins west of the outcrops. Palynology is used extensively in correlating these reservoirs and provides important evidence of age, presence of unconformities, changing climate and depositional conditions. Planned Itinerary Thurs 6 Jan: Depart Muscat at 7.00am. Travel via Sinaw to Huqf with brief stops enroute. Lunch in Huqf. Arrive Boy mid afternoon. Boy residual boulder spreads. Onward to A l Khlata S wadi. Remainder of afternoon in Al Khlata S wadi. Camp overnight Al Khlata. Fri 7 Jan: Al Khlata S w adi, Al Khlata boreholes, Al Khlata N wadi, Shab Nakhad wadis, Point Lookout, Ain Hindel. Camp overnight at Ain Hindel. Sat 8 Ja n: Ain Hindel pavement. Haushi Limestone at Akaba Woolley. U Gha rif-L Khuff at Akaba Woolley. M and U Gh arif at wadi Gharif. Drive to Jaaluni Oryx Project headquarters. Late afternoon guided visit to oryx. Camp overnight at Jaaluni. Sat 9 Jan: Drive to blacktop and on t owards Muscat. Brief stops at Qarat al Milh, Adam etc. to view geology. Arrive back in time to attend ‘icebreaker’ at Grand Hyatt.
Acknowledgement: The Ministry of Oil and Gas, and PDO, are thanked for their agreement to release data included in thi s guide.
Please note: The outcrops to be visited lie within the Arabian Oryx Sanctuary, a UN ESCO World Heritage Site. Permission has to be sought to v isit the area, currently from Dr Andrew Spalton (Office of the Conservation Advisor, Diwan of the Royal Court)
[email protected]. Please provide details of vehicles, proposed routes and campsites that will be p assed on to the Oryx Project Rangers at Jaaluni. To find out more about the project go to www.oryxoman.com Cover photos- Top- Oryx grazing ‘on the Gharif’, west of Bahama, Dec. 2004, Base- Ain Hindel pavement, variety of g lacial erosional features on Buah carbonates, Left- probable copepods from pitch clast found in d iamictite at Al Khlata, Right- spiriferid brachiopods in Haushi Limestone near Akaba Woolley.
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Outcrops to be visited
Strat interval of interest
Outcrops to be visited
Al Khlata and Gharif
Location map, stratigraphic column and regional cross section from Loosveld et al. (1996).
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Turn off wadi Shuram (E575422, N2228040)
Camp 6 (X)
7 7
8
5
4 9
3 Camp 2 Turn off to wadi Dungart (E566963, N2181396)
Duqm where IPC field party landed Feb. 1954, with the goal of reaching J. Fahud
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5
Haushi Lst (Saiwan Fm)
Masirah Bay Ss
HAIMA NAFUN Gp
Angudan unconformity
Part of PDO map (and legend) of the Huqf published in 1986. Its was based on a Petroleum Development Oman map from the 1960s. As it was made from unreferenced aerial photos it lacks coordinates. Planned stops numbered 1-9. Some older diagrams used in this guide have different numbers from Heward and Lopez Lopez (1984), ignore them.
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Buah
Jaaluni (E510471, N2205209)
Shuram
Khuff
Gharif Khufai
Al Khlata Jurf Plateau of Middle Miocene Fars Gp Qishn ~Shuaiba
Nahr Umr Samhan
BRGM map Sheet NE40-03/07 Duqm and Ras Madraca.
Jurf & Shuaiba Gharif
Al Khlata
Abu M
Khufai
Cross section from BRGM map Sheet NE40-03/07 Duqm and Ras Madraca. Note the pinching out of units onto the Huqf area which has been an uplift since the Proterozoic.
Duqm
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Haushi
Bai
The earliest description of the Al Khlata, albeit in passing is in Thesiger (1948). In the latter phase of his first crossing of the Empty Quarter in October 1946 - May 1947 he travelled via the Huqf depression from Haushi in the north to Bai in the south. “Then for two days we struggled across sabkhas, breaking through the surface crust at every step and floundering in the soft damp undersand. The infrequent ridges were chiefly composed of limestone, but here for the first time we found outcrops of red granite and of gabbro and many fragments of porphyry, jasper and rhyolite.” The igneous rock are Al Khlata boulders and one wonders whether the limestone ridges described are those of the Lower Gharif Haushi Limestone too?
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Outline structural geology from Ries and Shackleton, (1990). The N-NNW faults are a basement grain, often reactivated, the WSW-ENE broad folds are Angudan (M-Late Cambrian) and the Nafun-Haushi-Maradi fault zone (red) shows repeated strike-slip movement and formation of folds at Haushi, Buah and Mukhaibah.
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KHUFAI
KHUFAI
AL KHLATA
Al Khlata North wadi
Camp
Al Khlata South wadi
KHUFAI GHARIF
AL KHLATA
Annotated satellite image of the Al Khlata N and S wadi area. The + are 4 km apart. The Al Khlata infills a gentle syncline in the underlying Khufai and comprises mainly P5 glacial lake diamictites and silts, and glacial river sands and gravels. The red short lines above represent the orientation of striations on underlying glacial pavements and the arrows flow directions of large glacial meltwater rivers. BH = borehole. Boundaries of the glacial river deposits from Martin (1995). PDO have used these outcrops for 20 years for educating its staff about the nature of the Al Khlata.
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Sketch cross section of the Al Khlata N and S wadi area. The Al Khlata infills a syncline in the underlying Khufai and comprises mainly P5 glacio lacustrine diamictites and silts, and glaciofluvial sands and gravels. Palynofacies interpretations from the Al Khlata boreholes (modified from Knight and Penney, 1997) Haushi Limestone- (Permian Late Sakmarian). Age from brachiopods and fusulinids.
Upper silty sand…sim to U Mass Diamict. P1A (Permian Late Asselian). U M assive Diamict- P1A (Permian Late Asselian), relatively well-oxygenated conditions, prolific pteridophyte spores, clear mixing of lowland and upland palynomorphs. Warmer and wet. High proportion of fragmented palynomophs possibly indicating reworking. Upper heterolithic unit- ?Late P5/P1 (Permian Late Asselian), w ell preserved, macroscopic plant debris present in cores. SOM absent. Clear mixing of upland and lowland floral elements. Wind transported upland floras gymnosperm and cordiate spores indicating relatively cold and dry climate. Pteridophyte material possibly moist vegetation in vicinity of lakes. Unique and distinctive character. N&S wadi pebbly/sand units poor yields. (Late P5 Mid Asselian) Middle Silt- Late P5 (Permian Mid Asselian), d iverse ornamented pteridophyte spores, relatively moist conditions and traces of upland floras indicating cooler drier conditions. Recovery from slumped units poor. Lr Stratif Diamict- less SOM, more oxygenated and higher energy. Relatively diverse palynofloras as below, may be reworked. Less well oxygenated upwards. Lr Massive Diamict- Early P5 (Carboniferous Late Kasimovian/Stephanian). S OM prone, prob anoxic and low energy. Overall recovery relatively sparse, characterised by lowland pteridophyte spores- warmer (temperate) and moist. Not possible to rule out that palynomorphs reworked.
P9- (Carboniferous Westphalian – S tephanian). Absent from the outcrops at Al Khlata. Present in wells in and near the outcrops at Saiwan and Saih Hajmah.
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Horriditriletes ramosus
Microbaculispora tentula
Spores (and pollen) recovered from preparations of Al Khlata diamictites and shales and which provide a timeframe, allow correlation of this complex interval, and provide evidence of environment and climate. In the Al Khlata, most seem reworked from interglacial episodes (photos from Stephenson et al., 2003).
P1
P5 P9
Haushi Group (Al Khlata and Gharif) - Unayzah stratigraphy from Stephenson et al. (2003). The discovery in May 2004 of fusulinids in cores of the Haushi Limestone have confirmed its age as Late Sakmarian rather than Artinskian. Units P1, P5 and P9 stem from computer codes for dominant types of spores and pollen!
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Summary of Gondwanan glacial record from Crowell (1999). Al Khlata deposits range in age from Carboniferous-Westphalian to Permian-Sakmarian and correspond to times of maximum ice extent. The Late Sakmarian Haushi Limestone (Saiwan Fm of BRGM) may reflect the global sea level high as a result of deglaciation. Globes below are palaeogeographic reconstructions for the Early Carboniferous and Permian from Crowell. The location of Oman is indicated by an arrow. Makes one wonder why Oman was not icecovered in the Early Carboniferous?
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Early P5 Massive Diamictite
50°
Striations on the main P5 age (Permian) glacial pavement at Al Khlata. The striated substrate is smoothed Khufai dolomites and cherts (E545780, N2185370). Crag and tail implies ice movement to the NE.
Pleistocene terrace gravels
Al Khlata South Wadi Campsite
South Wadi sands and gravels AL KHLATA
Early P5 Late P5
KHUFAI
Section along the wadi walls of the upper part of the South wadi by John Martin (1995).
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Exposures used by PDO to demonstrate characteristics, log response and lateral extent of typical Al Khlata lithologies. Without palynology how would we recognise the ‘unconformity’ between the Early and Late P5 deposits. Cemented Recent Gravels
Late P5 South Wadi Sands and Gravels
Early P5 Lower Massive Diamictite
E545624, N2185376
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24 mm
26 mm
Clast pebble-sized 4-5 cm, ang-subround, dull slightly weathered exterior, shiny microfractured interior, low density (light), smells of tar when held over flame
Fragments with appendages are about 30-100 microns
Pitch (bitumen) clast discovered by Gion Kuper (Univ of Utretch) in January 2004 in P5 Massive diamictite at Al Khlata S wadi, N fork. Implies an active seep in S Oman during the Late Carboniferous. Geochemically, no evidence of biodegradation, and isotopes and biomarkers imply mix of intra-and pre-salt sources. Also yields abundant arthropod debris, probably copepods, but no spores or pollen as yet. If they are copepods then oldest known by >200Ma. Geochem- Paul Taylor (SIEP), Paly processing- Mike Stephenson (BGS), copepod interpretation by Paul Sheldon and Bill Spear (Univ of Manchester).
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A series of exposures at EOR or infill well spacings used by PDO to demonstrate lateral variability in the Al Khlata and the key importance of palynology in helping unravel the stratigraphy.
Striae Striae
Striae
Striae
E544746, N2184585 Steps on the Khufai dolomite surface and a number of areas with striations in the centre of the South wadi at Al Khlata. View looking north. Rare fine striae at 30° cut but fine-coarse ones oriented 55-70°. Striae often preserved or emphasised by iron pan on the contact between the Khufai carbonates and the Al Khlata.
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Ground penetrating radar (GPR) profiles recorded by Charlie Bristow (in Martin, 1995).
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E543700, N2184565
Al Khlata South wadi
TOP
BASE Due to the limited success of the GPR a series of shallow boreholes were cored and drilled. These were used to determine what lay between the outcrops and to calibrate the GPR data. They also provided a superb source of unweathered material for palynology (Martin,1995).
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E543397, N2185982 Al Khlata North wadi
TOP
BASE
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Al Khlata North wadi Late P5 North wadi Gravels passing downstream into Sands. Loaded into by pods of P1 Upper Massive Diamictite E545122, N2188078
Al Khlata North wadi Late P5 Remnant boulders from North wadi Sands and Gravels E543501, N2186289. These were powerful outwash rivers!
Al Khlata North wadi Late P5 Major scour at base of North wadi Sands and Gravels E544099, N2186790. Outcrop has also been interpreted as a Gilbert-type delta
Al Khlata North wadi Early P5 Lower Stratified Diamictite E544099, N2186790
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Base map from Levell et al. (1988)
Ice movement directions for Permo-Carb. glacial deposits in Africa and S Arabia (from Visser, 1997). Arrow for the Al Khlata added. Oman
Ice flow direction from striated pavements E Flank oil cf. with pitch clast
Batain Basin Late Carb rifting
Al Belushi et al. (1996)
Map from Immenhauser et al. (2000) most likely ice-movement direction indicated
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(Konert et al., 2001)
(Osterloff et al., 2004)
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Depositional model for the Al Khlata in South Oman from Levell et al. (1988).
Unconformities with a few hundreds of metres of erosion separate Al Khlata deposits in South Oman. Often these have the form of N or NW oriented outwash valleys which probably drained large lakes above areas of salt didissolution. A=P9, B=P5, C+Rahab=P1 (Heward, 1990).
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SHURAM Bahama QISHN KHUFAI Shab Nakhad North
Haushi Limestone GHARIF
To wadi Gharif
Furthest S outcrop of Haushi Lst
AL KHLATA
Shab Nakhad Central
Shab Nakhad South
KHUFAI
KHUFAI
Al Khlata North wadi Annotated satellite image of the Shab Nakhad area. The + are 4 km apart. The Al Khlata infills fault bounded topography in the underlying Khufai and is mainly P5? glacial lake deposits. We don’t yet have definitive age(s) for these outcrops. The red short lines above represent the orientation of striae on pavements and the arrows flow directions of climbing ripples and solemarks of density-flow deposits.
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KHUFAI
110° 20°
60°
?
240°
striae
Rock step at Shab Nakhad North, the main feature used by Heward (1990) and Al Belushi et al. (1996) to argue for ice flow to the south west. Heward was convinced by other lines of evidence of north easterly flow in the early ‘90s. Orientation of striae suggest pavement of P5 age (E545184, N219485).
Crack-fills of uncertain origin in a sequence of diamicts and sands at Shab Nakhad North. Inset photo of perigalcial patterned ground from western Iceland.
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Problematic crack fills, burrows, solemarks and pyrite rosettes now replace by heamatite? Probable P5 interglacial lake sequence at Shab Nakhad North (E545000, N2195488).
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Brown, sediment-laden meltwater entering lake (Jukulsarlon, south east Iceland).
Glacial lake deposits and different types of depositional environments and processes that may occur (after Ashley et al., 1985).
E544327, N2195488 Different types and sequences of climbing ripple cross-lamination are typical of glacial delta and lake deposits due to the high suspended sediment content of glacial meltwaters. Flow from left to right.
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Typical plan view of a pair of triliths, as at Shab Nakhad North. They are frequently encountered adjacent to wadis and tracks in Yemen, Dhofar, the Huqf, and the Oman Mountains (DeCardi et al., 1977). These monuments are considered pre-Islamic, late Iron Age constuctions. Sites labelled 7 and 8 below are in the Southern Huqf. There are several fine examples along the track between Wadi Boy (Buwi) and the Miocene escarpment en route to Al Ajaiz.
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Distinctive granite erratic boulder with large phenocrysts of feldspar. Weathered out of conglomerate or diamictite at the base of the Al Khlata north of Point Lookout (E545155, 2199989). Rests on Shuram. Likely derived from basement outcrops ?hundreds of kilometres away in Yemen/Saudi Arabia).
(base, Shaland et al., 2001)
No evidence of Al Khlata in Oman Mtns
Basement Ice movement directions
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E547000
AL KHLATA Turn off from N-S track (E546356, N2214303)
Camp
Grooves & striae
250m
BUAH
Grooves, striae & whalebacks N2214000
Annotated satellite image of the Ain Hindel pavement. The red lines above represent the orientation of large grooves and striae on the glacial pavement. The Al Khlata here has not been dated but the similarity in orientation of the features to those at Al Khlata (and Shab Nakhad) suggest it is Early P5.
View south east from the Camp across the Ain Hindel pavement with the Buah dipping at 7-15° NW beneath the sand-filled wadi in the foreground. Person for scale.
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5 m long large nailhead striation (E547187, N2214187)
30°
210°
E547139, N2214169
Long shallow grooves and striae orientated to 30-210°. The deep striae to the right narrows, deepens and the tool(s) that create it rotate out down the dipslope of the Buah. It leads into the large nailhead striation above. The implication is of ice moving to the north north east.
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Swarm of three small whalebacks within a 60m long, 2.5m wide, 0.75m deep groove orientated 30-210°. The whalebacks with their blunt upstream ends imply ice movement to the north north east. Photo from 1990, groove in 2004 quite sand filled (E547171, N2214063). Inset, Pleistocene whalebacks from the USA, ice movement from right to left.
30°
50°
60°
Three phase of ice movement indicated by striae to 60° (oldest), 50° and striae and grooves to 30° youngest. Location to left hand side of bottom photo on previous page.
SW
NE
Haushi Lst ~600 m Al Khlata
Haima
Seismic line through Saiwan showing erosional valleys at base Al Khlata (ex PDO report by van Vliet)
2300000
2200000
Mapped distribution of Al Khlata deposits in the outcrops and thicknesses in nearby wells. The best outcrops of the formation occur in the southern Huqf where it overlies consolidated Huqf strata. Further north, where it overlies softer Haima sediments, the characteristic boulder spreads and poor outcrops prevail.
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500000
34
Depositional model for the Buah Formation in the Huqf area (from Cozzi). Prolonged basment highs like the Huqf are characterised by mid- inner ramp carbonates with large stromatolites and cross-bedded ooid and peloid grainstones. Many stromatolite mounds are elongate possibly due to tidal currents.
Large eroded stromatolite mounds near the Shuram/Buah boundary, many elongated 50-230° (54707?, N2210066).
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Rub-Al Khali basin
Batain basin
Uplifted rift margin? sediment source area (Stampfli et al.,1991) Schreurs & Immenhauser, 1999) Rifting extending down into E Africa Palaeogeographical setting of Oman during the Permian. The Gharif comprises shallow marine and coastal plain deposits on the flank of the Rub Al Kali basin. Neo-Tethys lay to the north and the sediment source area for the Gharif appears limited to the uplifted Huqf margin. The Haushi Limestone transgression seems likely to have entered the Rub Al Khali basin from Neo-Tethys.
Summary sketch of the Gharif deposits of Oman and equivalents in Saudi Arabia, in a diagram with the vertical scale in time rather than thickness. The M Gharif is typically ~70 m thick in Central Oman and the U Gharif ~100 m. Permian sea-level curves from Weidlich and Bernecker (2002).
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Akaba Woolley GHARIF
AL KHLATA
AL KHLATA
Haushi Limestone
SHURAM
GHARIF AL KHLATA Point Lookout
Bahama
KHUFAI
QISHN
GHARIF Shab Nakhad North
GHARIF
AL KHLATA Haushi Limestone
Annotated satellite image of the Bahama, south Akaba Woolley and north Shab Nakhad area.The feature formed by the Haushi Limestone is very obvious with the darker appearing Al Khlata below and the lighter M and U Gharif above.
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Al Khlata
Single Haushi Limestone parasequence and ?maximum flood shale near Akaba Woolley (E564925, N2322573). The apparent absence of P1 Al Khlata is of interest and will be followed up in future work.
ooids E542231, N2193642
iron ooids
mfs?
The Haushi Limestone (Saiwan Fm of BRGM) is thin in the S Huqf outcrops and is not tracible S of Gharif. In the subsurface it is a marker unit ~30-50 m thick forming the upper part of the L Gharif.
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Brachiopods (spiriferids) occurring in the Permian Haushi ‘Limestone’ between Mifrid and Akaba Woolley (E542891, 2199594). The brachiopod shells are separated (disarticulalated) and many seem to have lain around on the sea floor and been bored by barnacles, colonised by bryozoa, and possibly used as holdfasts by other brachiopods.
A BRGM name!
More restricted, stormy, broken
Most diverse Fusulinids
Very restricted cold or hi energy?
Lucia Angiolini (Univ of Milan) has worked extensively on the brachiopods in the Haushi Limestone (e.g. Angiolini et al., 2001, 2004). In May 2004 she also began work, with Mike Stephenson (BGS), on the faunas and palynology of subsurface core material. They identified fusulinids in cores from Wafra-6 and Hasirah-1. Three brachiopod assemblages are present- a low diversity Pachycertella omanensis one, a more diverse Punctocertella spinosa one and a less diverse, increasingly fragmented Neospirifer hardmani one. Subsurface faunas are less diverse, quieter water or alternatively ooidal shoal. In the S Huqf the thin Haushi Lst and absence of Basal Sands seems to reflect onlap.
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Loc
Depth (m)
d 13C (%o, PDB)
d 18O (%o, PDB)
Surf Surf Surf GN-2 GN-2 GN-2 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 W FA-6 ZL-11 ZL-11 HSR-10 HSR-10 HSR-10 HSR-10 HSR-10 MZN-1 MZN-1 GN-2 W FA-6 ZL-11 MZN-1
25 25 25 1726 1726 1726 1746 1911 1911 1913 1913 1913 1913 1915 1915 1918 1922 1922 2461 2462 2570 2572 2572 2576 2576 4581 4583 1726 1918 2462 4581
2.67 2.48 1.09 2.64 2.57 2.51 2.25 1.79 1.6 3.26 3.19 2.52 2.61 2.85 3.28 2.83 1.21 2.24 1.41 3.78 2.23 2.99 3.19 2.37 1.86 4.96 4.89 3.47 4.49 4.46 5
-5.5 -4.17 -4.22 -6.42 -6.81 -7.68 -3.69 -5.43 -6.61 -3.62 -4.52 -5.65 -5.6 -5.38 -5.51 -6.59 -6.72 -7 -9.81 -6.44 -4.13 -6.82 -6.52 -8.17 -6.9 -3.9 -4.25 -2.46 -1.68 -2.11 -2.61
Comments from Paul Wright May 2003- Brachiopod shell material a bit heavy in C (+3 to +5) but there are other L Permian examples with heavy C so probably not an issue. What is a little odd are the whole rock values which show a typical shift in O but not C. Probably means that diagenesis was a closed system so that burial makes the O lighter (temp effect) but the C remains unaltered (the Haushi Lst would have been VERY unstable because of the high aragonite content - which seems very odd when you consider the lsts were buried by a fluvial package. Maybe the M Gharif was too arid and formed a seal isolating the Haushi Lst from later meteoric groundawaters Plotting O18 vs depth though shows quite a wide range of values per well or per area
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Large inclined burrow
Red subaqueous lacustrine deposits with burrows and desiccation cracks in the U Gharif of wadi Gharif. Some of the burrows are large and may well be vertebrate or crustacean ones ( W of loc. 7 on map below).
E539706, N2191958 Laterally varied and heterolithic channel-belt sands and intervening paleosols in the outcropping U Gharif at wadi Gharif. The sands in the S Huqf outcrops appear a mix of perennial and ephemeral river deposits.
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Heterolithic channel-belt sands from the U Gharif of wadi Gharif. The channel sands appear laterally accreted with sand and shale interbeds and abundant desiccation cracks probably indicative of ephemeral flows.
E538702, N2201873 Silicified tree trunk occurring in-situ within sands and silts (solid red oval) and occurring as fragments in wadi floor. Such fossil wood is typical of the Permian U Gharif where some trunks are up to 25 m long and are several dm in girth. They appear to be upland conifers, washed down rivers and silificied before burial and compaction. Growth rings indicate a seasonal climate. Uppermost Gharif/Khuff transition at Akaba Woolley.
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Pleistocene gravels Khuff
Outer ramp ‘epeiric sea’ storm deposits
Gharif
Coastal plain river deposits and paleosols
Upper Gharif and L Khuff outcrops in the North Cliffs area. The Khuff sea deepens rapidly, with Zoophycos trace fossils occurring about 5 m above the top of the Gharif. One wonders whether it was silled?
2300000
2200000 500000
Mapped distribution of Gharif deposits in the outcrops and thicknesses in nearby wells. The best outcrops of the formation occur in the southern and northern Huqf where it is overlain by consolidated Jurf or Lower Khuff carbonates. Often the Haushi Limestone forms a readily identifiable low topography and the Gharif is marked by its red detritus.
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Reference list, not all cited in guide; Al-Belushi, J.D., Glennie, K.W. and Williams, B.J.P., 1996. Permo-Carboniferous Al Khlata Formation, Oman: A new hypothesis of origin of its glaciation. GeoArabia, 1, 389-404. Al-Marjeby, A. and Nash, D., 1986. A summary of the geology and oil habitat of the Eastern Flank Hydrocarbon Province of SouthOman. Marine and Petroleum Geology, 3, 306-314. Angiolini, L., Platel, J-P., Roger, J. and Tintori, A., 2001. Lower to Middle Permian sedimentation on the Arabian platform: The succession of t he Haushi-Huqf area (Interior Oman). International Conference Geology of Oman, January 2001, Excursion A02. Angiolini, L., Crasquin-Soleau, S., Platel, J-P., Roger, J., Vachard, D., Vaslet, D. and Al-Husseini, M., 2004. Saiwan, Gharif and Khuff formations, Haushi-Huqf uplift, Oman. In : M . Al-Husseini (ed), Late Carboniferous-Early Triassic Arabian Plate Stratigraphy. GeoArabia Spec. Pub. 3, 149183. Ashley, G.M, Shaw, J. and Smith, N.D., 1985. Glacial Sedimentary Environments. SEPM Short Course 16. Besems, R.E. and Schuurman, W.M.L., 1987. Palynostratigraphy of Late Paleozoic glacial deposits of the Arabian Peninsula with special reference to Oman. Palynology, 11, 37-53. Blendinger, W., van Vliet, A. and Hughes Clarke, M.W., 1990. Updoming, rifting and continental margin development during the L ate Palaeozoic in northern Oman. In: Robertson, A.H.F., Searle, M.P. and Ries, A.C. (eds), The Geology and Tectonics of the Oman Region. Geological Society of London Spec. Pub. No. 49, 27-37. Braakman, J.H., Levell, B.K., Martin, J.H., Potter, T.L. and van Vliet, A., 1982. Late Palaeozoic Gondwana glaciation in Oman. Nature, 299, 2 September, 48-50. Crowell, J.C., 1999. Pre-Mesozoic ice ages: Their bearing on understanding the climate system. Geol. Soc. America Memoir 192, 106p. De Cardi, B, Doe, D.B. and Roskams, S.P., 1977. Excavation and survey in the Sharqiyah, Oman, 1976. The Journal of Oman Studies, 3, 1, 17-33. Guit, F.A., Al-Lawati, M.H. and N ederlof. P.J.R., 1994. Seeking new potential in the Early-Late Permian Gharif play, west Central Oman. In: M.I. Al-Husseini (ed) Geo’94, Gulf PetroLink, Manama, 447-462. Hartmann, B.H., Ramseyer, K. a nd Matter, A., 2000. Diagenesis and pore-water evolution in Permian sandstones, Gharif Formation, Sultanate of Oman. Journal of Sedimentary Research, 70, 533-544. Heward, A.P. and Lopez Lopez, J.A., 1984. Outcrops at Al Khlata and Gharif. PDO, Production Geology Field Guide 84/66, November 1984. Heward, A.P., 1990. Salt removal and sedimentation in Southern Oman. In: A.H.F. Robertson, M.P. Searle, and A.C. Ries (eds), The Geology and Tectonics of t he Oman Region. Geol. Soc. Spec. Pub., 49, 637-651. Hughes Clarke, M.W., 1988. Stratigraphy and rock unit nomenclature in the oil-producing area of interior Oman. J. Petrol. Geol., 11, 5-60. Immenhauser, A., Schreurs, G, Gnos, E., Oterdoom, H.W. and Hartmann, B., 2000. Late Palaeozoic to Neogene geodynamic evolution of the northeastern Oman margin. Geol. Mag., 137, 1-18. King, L.C., 1958. Basic palaeogeography of Gondwanaland during the Late Palaeozoic and Mesozoic eras. Q. J. Geol. Soc. Lond., 114, 47-77. Konert, G., Afifi, A.M., Al-Hajri, S.A. and Droste, H.J., 2001. Paleozoic stratigraphy and hydrocarbon habitat of the Arabian Plate. GeoArabia, 6, 407-442.
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Loosveld, R.J.H., Bell, A. and Terken, J.J.M., 1996. The tectonic evolution of I nterior Oman. GeoArabia, 1, 28-51. Martin, J.H., 1995. Al Khlata Formation integrated outcrop analogue study. Report for PDO, October 1995, 3 volumes. Morton, D.M., 1959. The geology of O man. Proc. 5th World Petroleum Congr., 1, 277-294. Osterloff, P., Penney, R., Aitken, J. a nd Clark, N., in press. Depositional sequences in the Al Khlata Formation, subsurface Interior Oman. In : M. Al-Husseini (ed), Late Carboniferous-Early Tertiary Arabian Plate Stratigraphy. GeoArabia Spec. Pub. 3 (due March 2004). Ries, A.C. and Shackleton, R,M., 1990. Structures in the Haushi-Huqf uplift, east Central Oman. In: A.H.F. Robertson, M.P. Searle, and A.C. Ries (eds), The Geology and Tectonics of the Oman Region. Geol. Soc. Spec. Pub., 49, 653-664. Schreurs, G. and Immenhauser, A., 1999. West-northwestward directed obduction of th e Batain Group on the eastern Oman continental margin at the Cretaceous-Tertiary boundary. Tectonics, 18, 148-160. Stephenson, M.H., Osterloff, P.L. and Filatoff, J., 2003. Palynological biozonation of the Permian of Oman and Saudi Arabia: progress and challenges. GeoArabia, 8, 467-496. Thesiger, W., 1948. Across the Empty Quarter. The Geographical Journal, 111, 1-21. Weidlich, O. and Bernecker, M., 2002. Supersequence and composite sequence carbonate platform growth: Permian and Triassic outcrop data of the Arabian platform and Neo-Tethys. Sedimentary Geology, 158, 87-116.
Participants List: Alan Heward
Petroleum Development Oman
[email protected]
Omar Al Ja’aidi
Sultan Qaboos Centre, Oman
[email protected]
Saleh Al Anboori
Ministry of Oil and Gas, Oman
[email protected]
Bader Al Sariri
Ministry of Oil and Gas, Oman
[email protected]
Beniot Beauchamp
Geological Survey Canada, Calgary
[email protected]
Erin Lamb-Fauquier
EnCana, Calgary
[email protected]
Carmen Neufeld
EnCana, Calgary
[email protected]
Robert MacDonald
EnCana, Calgary
[email protected]
Joe Martin
Manchester Univ, UK
[email protected]
Chris Willan
Exxon-Mobil
[email protected]
Alain Guidou
Petroleum Development Oman
[email protected]
Edmund Huang
Petroleum Development Oman
[email protected]
Sami Al Nofli
Petroleum Development Oman
[email protected]
Univ,
Carbonate
