438:, marks a change in fault polarity from NE-dipping in the Darag Basin to the north to SE-dipping to the south in the Belayim province. It coincides with the location of the Cretaceous inversion structure, the Wadi Araba anticline. It has been suggested that the presence of this structure acted as a barrier to northward propagation of the rift. Its location may also be partly controlled by the Rehba Shear Zone in the underlying basement.
415:
114:
338:
20:
394:(late Early Miocene, c. 18 Ma). In the Middle Miocene break-up occurred along the whole length of the Red Sea rift with seafloor spreading beginning in the Late Miocene. This break-up was associated with a gradual reduction in the rate of rifting along the Gulf of Suez with most activity stopping by the beginning of the Pliocene.
446:
The Morgan accommodation zone marks a switch in fault polarity from NE-dipping to the north to SW-dipping to the south in the Amal-Zeit province. It also coincides with a marked southward widening of the rift zone. There is no earlier structure known that influenced the location of this accommodation
280:
age limestones of either the Thebes or
Waseiyit Formations. Together with the middle to late Eocene Mokattam Formation this sequence reaches a combined maximum thickness of 500 m. These limestones are followed by continental to locally shallow marine red sandstones of the Tayiba Formation, which
101:. This model is consistent with near orthogonal rifting along the entire length of the rift system. Alternative models that suggest initiation by strike-slip faulting and pull-apart basin development along the axis of the rift have not been supported by detailed studies of the rift geometry.
308:
The deepening of the rift is recorded by the lower
Miocene Rudeis Formation. The lower part, consisting of marls and sandstones, is overlain by coarse sandstones and conglomerates reflecting a rapid increase in rift topography at that time. The Kareem Formation saw the first development of
190:. These sequences then pass up into the sandstones of the Abu Thora Formation. In the northern Gulf, at Wadi Araba, the early Carboniferous is overlain by upper Carboniferous of the Rod e Hamal, Abu Darag and Ahmeir Formations. In the southern Gulf the Carboniferous strata are capped by
501:
The best quality reservoir in the Gulf of Suez is the mainly Lower
Cretaceous Malha Formation, sometimes known as the 'Nubia' or 'Nubian A'. This pre-rift sequence is present throughout the gulf, and has porosities in the range 13–29 % with permeabilities varying from 70 to 400
325:
limestones of the uppermost middle
Miocene Belayim lie unconformably on the Kareem. More restricted basin conditions continued with the upper Miocene South Gharib and Zeit Formations with deposition of halite with some anhydrite and mudstone, representing the last syn-rift deposits.
514:
The dominant play type in the Gulf of Suez is tilted fault blocks with pre-rift Early
Cretaceous sands sealed by syn-rift sequences and source from the Duwi limestone. Additional discoveries have been made in a wide range of structural, stratigraphic and combined play types.
251:
strata. The
Campanian Duwi Formation, known as the Brown Limestone, was deposited throughout the gulf apart from the uplifted area of the North Galala plateau and Wadi Araba where it is replaced by chalk of the Thelmet Formation. These pass up into Sudr Formation chalks of
173:
units have a combined thickness of about 500 m. They were deposited in a continental environment except in the northeastern part of the gulf where they become marine. The next preserved sequence is the Umm Bogma or Abu Durba
Formations of lower
353:
pre-rift carbonate (source rock); N, R, K, and B = syn- and post-rift Nukhul, Rudeis, Kareem and
Belayim formation (sources, reservoirs, seals and overburden); SG = South Gharib salt (seal and overburden); Z=Zeit (seals and overburden); and PP =
484:
content (TOC) of 2.6 wt% with some samples measuring up to 21 wt%. In the southern part of the gulf, the
Miocene source intervals become important as higher geothermal gradients cause parts of the syn-rift sequence to reach maturity. Marine
475:
in the Gulf of Suez is the
Campanian age Brown Limestone or Duwi Member of the Sudr Formation. This unit is typically 25–70 m thick and is distributed from the southern end of the gulf as far north as Wadi Araba. It contains mainly type II
523:
The Gulf of Suez rift has been intensively studied by academic groups and by companies as analogue for rift basins in general. This is due to the generally good exposure within the onshore part of the rift coupled with the availability of
300:
of the Nukhul Formation were deposited in shallow marine conditions as the sea began to flood the developing rift. The Nukhul Formation overlies the Abu Zenima Formation in some place but elsewhere is probably age equivalent, reflecting a
104:
Towards the end of the Miocene, the Arabian Plate began to collide with the Eurasian Plate leading to changes in the plate configuration, the development of the Dead Sea Transform and cessation in rifting in the Gulf of Suez.
792:"Late Cretaceous (c. 84 Ma) compressive deformation of the stable platform of northeast Africa (Egypt): Far-field stress effects of the "Santonian event" and origin of the Syrian arc deformation belt"
379:
structures. These structures were mainly active during the Late Santonian but there is evidence of further movements on the same structures at the end of the Cretaceous and during the Paleogene.
153:. These rocks contain shear zones, such as the Rehba Shear Zone of western Sinai, that are interpreted to have partly controlled the orientation and location of rift structures.
1038:
329:
The Pliocene–Recent postrift sequence reaches up to 2000 m in thickness in the southern part of the rift and is formed of interbedded sandstones, limestones and evaporites.
565:
Khalil, S.M.; McClay K.R. (2001). "Tectonic evolution of the NW Red Sea-Gulf of Suez rift system". In Wilson, R.C.L.; Whitmarsh, R.B.; Taylor, B.; Froitzheim, N. (eds.).
1214:
943:
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Rifting began along the whole of the Red Sea -Gulf of Suez rift system during the Late Oligocene. In the Gulf of Suez rift, the rifting culminated during the
1179:
991:
224:
age. These sandstones are up to 400 m in thickness, form an important reservoir in the Gulf of Suez and are known informally as the 'Nubian' sandstone.
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1189:
1355:
1209:
1031:
1335:
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838:"Carbonate Platform to Basin Transition along an Upper Cretaceous to Lower Tertiary Syrian Arc Uplift, Galala Plateaus, Eastern Desert of Egypt"
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698:
78:
178:
age, which sit apparently conformably on the Cambrian, although the base represents a hiatus of about 150 Ma. The Umm Bogma Formation is
1443:
1433:
1360:
313:, indicating basin restriction, followed by open marine shales, as coarse clastic deposition began to reduce in the middle Miocene. Shales,
1024:
247:
at the end of the Santonian. Structures such as Wadi Araba became uplifted at this time giving rise to folding and local erosion of pre-
209:
in age, although it is considered to include Permian strata near its base near Wadi Araba. The Qiseib Formation consists of sandstones,
426:
of alternating polarity. The changes in fault polarity and position from segment to segment are taken up by broad accommodation zones.
371:. This period was mainly quiet tectonically but the northern part of the gulf region was affected by periodic far-field effects of the
205:
The Qiseib Formation is found throughout the Gulf varying in thickness between 8 m and 300 m. It is thought to be mainly
284:
The continental sandstones and siltstones of the Abu Zenima Formation represent the earliest syn-rift deposits of late Oligocene (
70:. During its brief post-rift history, the deepest part of the remnant rift topography has been filled by the sea, creating the
764:
670:
593:
576:
1370:
966:
1766:
375:. A series of WSW-ENE trending extensional basins were inverted, creating isolated uplifted and folded areas known as
1591:
341:
Generalised structural cross-section through the Gulf of Suez, just south of the Morgan Accommodation Zone. PZ-LK =
77:
North of the Gulf of Suez the rift becomes indistinct and its exact geometry uncertain, linking eventually to the
1771:
913:
815:
231:
Raha Formation, a sequence of interbedded shales limestones and sandstone, is succeeded by limestones of the
62:
until break-up occurred in the middle Miocene, with most of the displacement on the newly developed Red Sea
493:
Magna Formation is the most important of these younger source rocks with a TOC ranging from 1–2 wt %.
227:
The upper Cretaceous sequence consists of shallow marine deposits that generally thicken northwards. The
276:
age are represented by the Esna Shale Formation which overlies the Sudr Formation. This is succeeded by
93:
The formation of the Red Sea – Gulf of Suez rift system was caused by the anticlockwise rotation of the
1184:
1009:
USGS Open-File Report OF99-50-A The Red Sea Basin Province: Sudr-Nubia(!) and Maqna(!) Petroleum System
243:
age Matullah Formation. The central and northern parts of the gulf were locally affected by a phase of
918:
USGS Open File Report 99-50-A The Red Sea Basin Province: Sudr-Nubia(!) and Maqna(!) Petroleum Systems
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720:
367:
During the Late Cretaceous to Eocene, the area now occupied by the rift was a shallow sea depositing
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Since the end of the Miocene the area of the Gulf of Suez rift has begun to experience post-rift
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Continental rift zone that was active between the Late Oligocene and the end of the Miocene
8:
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944:"Petroleum geology and potential hydrocarbon plays in the Gulf of Suez rift basin, Egypt"
244:
856:
807:
671:"18 Structural and stratigraphic evolution of the Gulf of Suez Rift, Egypt: a synthesis"
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Cambrian rocks of Araba and Naqus Formations occur throughout the region above a planar
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1735:
1705:
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1257:
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Non-Volcanic Rifting of Continental Margins: A Comparison of Evidence from Land and Sea
459:
fields and discoveries have been reported from the Gulf of Suez rift with a variety of
403:
289:
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67:
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1016:
571:. Special Publication. Vol. 187. Geological Society of London. pp. 453–473.
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680:. Mem. Mus. natn. Hist. nat. Vol. Peri-Tethys Memoir 6. Paris. pp. 567–606
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The Qiseib Formation is overlain by the sandstones of the Malha Formation of upper
1531:
624:
1700:
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894:. Special Publications. Vol. 80. London: Geological Society. pp. 75–102
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182:, while the stratigraphically equivalent Abur Durba Formation consists of black
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721:"Development of Accommodation Zones in the Gulf of Suez-Red Sea Rift, Egypt"
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sequence was formed during the Campanian/Maastrichtian, continuing into the
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676:. In Ziegler P.A.; Cavazza W.; Robertson A.H.F.; Crasquin-Soleau (eds.).
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accompanied by flooding of the topographically lowest parts of the rift.
388:
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24:
30:
and linear rift structures are clearly visible on both sides of the gulf
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The Gulf of Suez rift is strongly segmented along its length with
477:
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235:
Wata Formation. This is overlain by sandstones and shales of the
191:
139:
55:
888:"A high-strain rift model for the southern Gulf of Suez (Egypt)"
113:
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wells and seismic reflection datasets within the gulf itself.
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10.1130/0091-7613(1999)027<0633:LCCMCD>2.3.CO;2
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39:
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age. On the southern margin of the uplifted Wadi Araba, a
23:
Satellite image of the Gulf of Suez, dark outcrops of the
1646:
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1046:
752:
518:
296:. The lower Miocene age conglomerates, sandstones and
349:
Nubia (reservoir rock); UK-EO = Upper Cretaceous to
292:) age. Locally the Abu Zenima Formation is capped by
790:
Bosworth, W.; Guiraud, R.; Kessler II, L.G. (1999).
591:
753:Tawadros, Edward; Ezzat Tawadros (2 January 2000).
678:
Peri-Tethyan Rift/Wrench Basins and Passive Margins
668:
835:
126:The basement consists of Precambrian rocks of the
990:: CS1 maint: DOI inactive as of September 2024 (
564:
213:at the base with an overall fining upward trend.
1748:
58:(c. 5 Ma). It represented a continuation of the
718:
592:Bosworth, W.; Huchon, P.; McClay, K.R. (2005).
429:
1032:
305:change to marine conditions within the rift.
281:represent the last of the pre-rift deposits.
937:
935:
441:
836:Kuss, J.; Scheibner, C.; Gietl, R. (2000).
785:
783:
737:10.1306/61EEDC10-173E-11D7-8645000102C1865D
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697:: CS1 maint: location missing publisher (
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892:Rift Structure: Models and Observations
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418:Structural map of the Gulf of Suez rift
1749:
450:
42:zone that was active between the Late
1020:
965:(inactive 2024-09-13). Archived from
759:. Taylor & Francis. p. 500.
705:
594:"The Red Sea and Gulf of Aden Basins"
585:
555:
117:Stratigraphy of the Gulf of Suez rift
1371:West and Central African Rift System
436:Galala-Abu Zenima Accommodation Zone
1047:Major African geological formations
906:
829:
519:Importance as a rift basin analogue
13:
669:Bosworth, W.; McClay K.R. (2001).
496:
14:
1783:
1002:
601:Journal of African Earth Sciences
719:Younes, A.I.; McClay K. (2002).
621:10.1016/j.jafrearsci.2005.07.020
466:
108:
1:
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509:
434:This zone, also known as the
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47:
430:Zaafarana accommodation zone
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409:
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10:
1788:
1767:Cenozoic rifts and grabens
1185:Central African Shear Zone
756:Geology of Egypt and Libya
382:
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66:being accommodated by the
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1562:Central Pangean Mountains
1522:
1384:
1291:
1223:
1215:Western Meseta Shear Zone
1165:
1103:
1052:
442:Morgan accommodation zone
942:Alsharhan, A.S. (2003).
865:10.2113/geoarabia0503405
526:hydrocarbon exploration
1772:History of the Red Sea
1582:Eastern Rift mountains
1504:Tanzania Coastal Basin
1283:Terra Australis Orogen
419:
359:
169:. These red and white
118:
89:Plate tectonic setting
31:
1597:Great Karas Mountains
1577:Eastern Arc Mountains
1117:Arabian-Nubian Shield
886:Bosworth, W. (1995).
417:
340:
128:Arabian-Nubian Shield
116:
54:) and the end of the
28:Arabian-Nubian Shield
22:
1494:Somali Coastal Basin
1205:Mwembeshi Shear Zone
963:10.1306/062002870143
482:Total organic carbon
288:) to early Miocene (
97:with respect to the
1672:Teffedest Mountains
1587:Ethiopian Highlands
1278:Pan-African orogens
1248:East African Orogen
1180:Broodkop Shear Zone
1152:West African Craton
1095:Victoria Microplate
857:2000GeoAr...5..405K
808:1999Geo....27..633B
613:2005JAfES..43..334B
480:and has an average
451:Economic importance
1736:List of inselbergs
1706:Jugurtha Tableland
1657:Sankwala Mountains
1652:Rwenzori Mountains
1469:Ouled Abdoun Basin
1464:Orange River Basin
1386:Sedimentary basins
1195:Foumban Shear Zone
1137:Saharan Metacraton
420:
404:thermal subsidence
360:
119:
68:Dead Sea Transform
32:
1744:
1743:
1677:Tibesti Mountains
1637:Mitumba Mountains
1627:Mandara Mountains
1612:Imatong Mountains
1567:Chaillu Mountains
1547:Bambouk Mountains
1484:Rio del Rey Basin
1454:Niger Delta Basin
1439:Iullemmeden Basin
1331:Gulf of Suez Rift
1326:East African Rift
1311:Bahr el Arab rift
1258:Gondwanide Orogen
1190:Chuan Shear Zones
766:978-90-5809-331-8
578:978-1-86239-091-1
38:is a continental
36:Gulf of Suez Rift
1779:
1632:Marrah Mountains
1607:Hoggar Mountains
1602:Guinea Highlands
1592:Great Escarpment
1356:Sangha Aulacogen
1273:Mauritanide Belt
1200:Kandi Fault Zone
1175:Aswa Dislocation
1090:Seychelles Plate
1080:Madagascar Plate
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1034:
1027:
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731:(6): 1003–1026.
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623:. Archived from
607:(1–3): 334–378.
598:
589:
583:
582:
562:
356:Plio-Pleistocene
138:are intruded by
134:, volcanics and
64:spreading centre
49:
1787:
1786:
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1780:
1778:
1777:
1776:
1747:
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1701:Mount Gorongosa
1681:
1542:Aurès Mountains
1537:Atlas Mountains
1524:Mountain ranges
1518:
1404:Blue Nile Basin
1380:
1376:White Nile rift
1287:
1253:Eburnean Orogen
1219:
1210:Todi Shear Zone
1161:
1157:Zimbabwe Craton
1142:Tanzania Craton
1132:Kalahari Craton
1127:Kaapvaal Craton
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972:on 14 July 2011
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543:Sinai Peninsula
538:Isthmus of Suez
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497:Reservoir rocks
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461:petroleum plays
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146:and a suite of
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1642:Nuba Mountains
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1622:Loma Mountains
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1336:Lamu Embayment
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1321:Blue Nile rift
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1303:
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1263:Kibaran Orogen
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1238:Cape Fold Belt
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851:(3): 405–424.
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1758:
1755:
1754:
1752:
1737:
1734:
1732:
1729:
1727:
1724:
1722:
1719:
1717:
1714:
1712:
1709:
1707:
1704:
1702:
1699:
1697:
1694:
1693:
1691:
1688:
1684:
1678:
1675:
1673:
1670:
1668:
1665:
1663:
1662:Serra da Leba
1660:
1658:
1655:
1653:
1650:
1648:
1647:Rif Mountains
1645:
1643:
1640:
1638:
1635:
1633:
1630:
1628:
1625:
1623:
1620:
1618:
1617:Jebel Uweinat
1615:
1613:
1610:
1608:
1605:
1603:
1600:
1598:
1595:
1593:
1590:
1588:
1585:
1583:
1580:
1578:
1575:
1573:
1570:
1568:
1565:
1563:
1560:
1558:
1557:Cameroon line
1555:
1553:
1550:
1548:
1545:
1543:
1540:
1538:
1535:
1533:
1532:Aïr Mountains
1530:
1529:
1527:
1525:
1521:
1515:
1514:Turkana Basin
1512:
1510:
1509:Tindouf Basin
1507:
1505:
1502:
1500:
1497:
1495:
1492:
1490:
1487:
1485:
1482:
1480:
1479:Reggane Basin
1477:
1475:
1472:
1470:
1467:
1465:
1462:
1460:
1457:
1455:
1452:
1450:
1447:
1445:
1442:
1440:
1437:
1435:
1432:
1430:
1427:
1425:
1422:
1420:
1417:
1415:
1412:
1410:
1407:
1405:
1402:
1400:
1397:
1395:
1392:
1391:
1389:
1387:
1383:
1377:
1374:
1372:
1369:
1367:
1364:
1362:
1359:
1357:
1354:
1352:
1349:
1347:
1344:
1342:
1339:
1337:
1334:
1332:
1329:
1327:
1324:
1322:
1319:
1317:
1314:
1312:
1309:
1307:
1304:
1302:
1301:Afar Triangle
1299:
1298:
1296:
1294:
1290:
1284:
1281:
1279:
1276:
1274:
1271:
1269:
1268:Kuunga Orogen
1266:
1264:
1261:
1259:
1256:
1254:
1251:
1249:
1246:
1244:
1243:Damara Orogen
1241:
1239:
1236:
1234:
1233:Alpine Orogen
1231:
1230:
1228:
1226:
1222:
1216:
1213:
1211:
1208:
1206:
1203:
1201:
1198:
1196:
1193:
1191:
1188:
1186:
1183:
1181:
1178:
1176:
1173:
1172:
1170:
1168:
1164:
1158:
1155:
1153:
1150:
1148:
1147:Tuareg Shield
1145:
1143:
1140:
1138:
1135:
1133:
1130:
1128:
1125:
1123:
1120:
1118:
1115:
1114:
1112:
1110:
1106:
1102:
1096:
1093:
1091:
1088:
1086:
1083:
1081:
1078:
1076:
1075:Lwandle Plate
1073:Microplates:
1072:
1070:
1066:
1064:
1063:African Plate
1060:
1059:
1057:
1055:
1051:
1042:
1037:
1035:
1030:
1028:
1023:
1022:
1019:
1015:
1010:
1007:
1006:
993:
987:
968:
964:
960:
956:
952:
951:AAPG Bulletin
945:
938:
936:
919:
915:
914:"Source Rock"
909:
893:
889:
882:
874:
870:
866:
862:
858:
854:
850:
846:
839:
832:
817:
813:
809:
805:
801:
797:
793:
786:
784:
768:
762:
758:
757:
749:
747:
738:
734:
730:
726:
725:AAPG Bulletin
722:
715:
713:
711:
709:
700:
694:
679:
672:
665:
663:
661:
659:
657:
655:
653:
651:
649:
647:
645:
630:on 2011-08-18
626:
622:
618:
614:
610:
606:
602:
595:
588:
580:
574:
570:
569:
561:
559:
554:
544:
541:
539:
536:
535:
529:
527:
516:
507:
505:
494:
492:
488:
483:
479:
474:
464:
462:
458:
448:
439:
437:
427:
425:
416:
407:
405:
395:
393:
390:
380:
378:
374:
370:
358:(overburden)
357:
352:
348:
344:
339:
330:
327:
324:
320:
316:
312:
306:
304:
299:
295:
291:
287:
282:
279:
275:
265:
263:
259:
255:
254:Maastrichtian
250:
246:
242:
238:
234:
230:
225:
223:
219:
214:
212:
211:conglomeratic
208:
198:
196:
193:
189:
185:
181:
177:
176:Carboniferous
172:
168:
164:
154:
152:
149:
145:
144:granodiorites
141:
137:
136:metasediments
133:
129:
115:
106:
102:
100:
99:African Plate
96:
95:Arabian Plate
86:
84:
80:
75:
73:
69:
65:
61:
57:
53:
45:
41:
37:
29:
26:
21:
1689:(aka koppie)
1474:Owambo Basin
1459:Ogaden Basin
1449:Murzuq Basin
1419:Douala Basin
1394:Angola Basin
1366:Urema Valley
1351:Red Sea Rift
1346:Muglad Basin
1330:
1316:Benue Trough
1122:Congo Craton
1085:Rovuma Plate
1069:Somali Plate
1013:
986:cite journal
974:. Retrieved
967:the original
954:
950:
922:. Retrieved
917:
908:
896:. Retrieved
891:
881:
848:
844:
831:
819:. Retrieved
799:
795:
770:. Retrieved
755:
728:
724:
682:. Retrieved
677:
632:. Retrieved
625:the original
604:
600:
587:
567:
522:
513:
500:
470:
467:Source rocks
454:
445:
435:
433:
424:half-grabens
421:
401:
386:
366:
328:
307:
283:
271:
226:
215:
204:
163:unconformity
160:
125:
109:Stratigraphy
103:
92:
81:beneath the
79:Manzala rift
76:
72:Gulf of Suez
60:Red Sea Rift
35:
33:
1572:Drakensberg
1489:Sirte Basin
1444:Kufra Basin
1434:Gabon Basin
1429:Karoo Basin
1414:Congo Basin
1361:Atbara rift
1341:Melut Basin
1306:Anza trough
1167:Shear zones
473:source rock
457:hydrocarbon
389:Burdigalian
303:diachronous
25:Precambrian
1762:Aulacogens
1751:Categories
1711:Mount Mabu
1696:Anti-Atlas
1687:Inselbergs
1409:Chad Basin
684:2010-04-27
634:2010-04-27
549:References
510:Main plays
377:Syrian Arc
369:carbonates
347:Cretaceous
311:evaporites
290:Aquitanian
229:Cenomanian
222:Cretaceous
157:Palaeozoic
83:Nile delta
1757:Tectonics
1731:Zuma Rock
1726:Wase Rock
873:128180958
845:GeoArabia
693:cite book
471:The main
398:Post-rift
345:to lower
343:Paleozoic
315:anhydrite
274:Paleocene
272:Rocks of
262:Paleogene
249:Campanian
245:inversion
241:Santonian
237:Coniacian
220:to lower
195:volcanics
188:mudstones
180:dolomitic
171:sandstone
44:Oligocene
1424:El Djouf
532:See also
410:Geometry
363:Pre-rift
286:Chattian
268:Cenozoic
233:Turonian
218:Jurassic
207:Triassic
201:Mesozoic
148:dolerite
140:granites
132:Gneisses
122:Basement
1225:Orogens
1109:shields
1105:Cratons
898:May 31,
853:Bibcode
804:Bibcode
796:Geology
609:Bibcode
489:of the
478:kerogen
383:Rifting
333:History
294:basalts
192:Permian
56:Miocene
1399:Aoukar
1054:Plates
976:17 May
920:. 1999
871:
821:15 May
772:15 May
763:
575:
447:zone.
351:Eocene
323:reefal
319:halite
278:Eocene
184:shales
1293:Rifts
970:(PDF)
957:(1).
947:(PDF)
924:7 May
869:S2CID
841:(PDF)
674:(PDF)
628:(PDF)
597:(PDF)
487:shale
392:stage
298:marls
151:dykes
1107:and
992:link
978:2010
926:2010
900:2010
823:2010
774:2010
761:ISBN
699:link
573:ISBN
321:and
186:and
40:rift
34:The
959:doi
861:doi
812:doi
733:doi
617:doi
130:.
50:28
1753::
988:}}
984:{{
955:87
953:.
949:.
934:^
916:.
890:.
867:.
859:.
847:.
843:.
810:.
800:27
798:.
794:.
782:^
745:^
729:86
727:.
723:.
707:^
695:}}
691:{{
643:^
615:.
605:43
603:.
599:.
557:^
506:.
504:md
463:.
317:,
264:.
197:.
142:,
85:.
74:.
52:Ma
48:c.
1040:e
1033:t
1026:v
994:)
980:.
961::
928:.
902:.
875:.
863::
855::
849:5
825:.
814::
806::
776:.
739:.
735::
701:)
687:.
637:.
619::
611::
581:.
239:-
46:(
Text is available under the Creative Commons Attribution-ShareAlike License. Additional terms may apply.
