Post-Karroo melilite basalts intrude Cretaceous and older sedimentary units in the Cape Province, South Africa. K-Ar ages determined from 4 occurrences range from 63–75 Ma b.p. (Late Cretaceous to earliest Tertiary) and are significantly older than alkaline intrusions to the 5, on the Alphard Bank. These igneous intrusions may be part of a linear trend that connects young oceanic volcanism at Bouvet Island with Cretaceous kimberlitic activity in southern Africa. This lineament nearly parallels the Walvis Ridge and a hot spot model for its origin is examined.

Thirty samples of Upper Tertiary basalts intruding marine and continental sequences were by the K-Ar method. Four volcanic phases are recorded: (a) 24.8±1.5 Ma of the Raqabat e Na'ame dike in Central Sinai; (b) 20.4±0.7 Ma of basalt intrusions in Central Sinai and the Arava. Some of these are offset by E-W to NE-SW dextral faults of the Central Sinai – Negev Shear Zone; (c) 14.5±0.3 to 4.9±1.3 Ma of basalt flows in the Eastern Galilee and the Coastal Plain; (d) 2.7±0.6 Ma of ‘En Yahav dike. These results contribute to the correlation between Tertiary continental formations from different areas, and put limits on the age of tectonic events, such as folding in the Syrian arc, faulting in the Central Sinai - Negev Shear Zone and shearing along the Jordan Rift.

Simple expressions given in terms of Mohr diagram parameters may be used both to check the accuracy of Mohr diagram constructions and/or to replace particular constructions in stress analyses of brittle rock failure. Examples of expressions relating to two common types of composite failure envelope are given together with brief examples of their possible application.

A trilobite fauna of Llandovery/Wenlock age is described. Five species are represented:Rhax polllnctrix gen. et sp. nov. (Scutelluidae), a warburgelline?, Sphaerexochus sp.,Encrinurus? sp., and a calymenid. The morphology of R. pollinctrix supports the view that Bumastus is a scutelluid, and consequently that the Illaenidae, as presently conceived, is polyphyletic.

Calcirudites in the Upper Devonian (Frasnian) of Central Poland are often couplets with a laminated intrapelsparite upper part and a lower section of intraformational calcarenitic and micritic flat pebbles. The pebbles are associated with bioclasts derived from 3 offshore environments: I, a fully marine area (echinoderms, rugose and tabulate corals, brachiopods, trilobites and conodonts); II, phytogenic banks (globose stromatoporoid stromatolites and Renalcis); III, restricted lagoons (ramose stromatoporoids, calcispheres, ostracodes and peloids). Many of the flat pebbles are only slightly displaced and had been partially cemented before being reworked. The depositional environment was subtidal. The considerable size of the flat pebbles and the complex nature of the surrounding matrix suggest that storm surges or tsunami may have disrupted beds and led to channelling and pebble formation.

There are close geometrical and dimensional similarities between the faults in Scotland north of the Highland Boundary Fault and faults in southern California east of the San Andreas Fault. It is argued that the Moine Thrust and Oarlock Fault are equivalents and that the Great Glen Fault and the Rosamund Lineament are also equivalent, implying corresponding senses of movement and that the Highland Boundary Fault originated as a dextral transform. The comparison cannot be extended yet to the terrains to the N of the Oarlock Fault or W of the San Andreas or to the corresponding areas in the Caledonides.

Two small outcrops of harzburgite and asbestos-bearing serpentinite, occurring S of Di Zahav in eastern Sinai are the first record of ultramafic rocks from the Sinai Precambrian massif.

Structures formed during wind deflation of poorly sorted beach sediments have rarely been described in the literature. However, a number of distinct forms exist including capped pedestals, asymmetrical ‘tear’ structures and scoured or impacted crusts. All these phenomena result from differential spatial erosion of the beach surface by wind, caused by textural or compositional variations. Ephemeral structures are indicative of rapidly changing geomorphological conditions and their presence may also exert control over continuing aeolian processes.