ment; but this cause does not seem probable, on account of the similarity in lithological character of both the Keuper and Bunter formations in distant countries. Perhaps the conglomerates at the base of our Keuper sandstone, may be the representatives of the Muschelkalk, though the usual absence of lime even as a cementing medium, certainly would not lead to such a conclusion. Again, the Bunter formation may have been dry land during the deposition of the Muschelkalk in more southern and easterly regions. If such were the case, some evidence should surely be visible in our immediate locality. Whatever view we may take of this important subject, the minute examination of the base of the Keuper formation is the only place where we can expect to find data towards solving the question. This explanation conveys a precise idea of the object of the present paper. Before proceeding to point out in detail the peculiarities of the Keuper, it is advisable to refer to the five subdivisions of the Trias. From the examination of my original line of section, taken from the river Dee to the rise of the coal measures east of Liverpool, all these sub-divisions can be coordinated, for in different parts of that line all can be observed under very favourable circumstances, and present the following order of sequence from the top downwards : ... Conglomerate beds of the Bunter ... ... ... In the maps of the Geological Survey the sub-divisions are coloured (excepting that the upper and lower Bunter are not separated,) and they are very useful in marking out the leading features of a district, though they must not be supposed to be absolutely correct, for local geologists are collecting from time to time new data from numerous artificial excavations, tending to correct them. It is to be hoped that means will be taken by the officers of the survey, to investigate such additions and improvements as may be necessary to make the maps accurate guides to local geology. I have alluded to this subject because my own map differs from that of the Geological Survey containing Liverpool; but as my sections have received the sanction of the geologist, Edward Hull, Esq., F.G.S., who originally surveyed the district, I expect that the result of my observations will be adopted in a new edition of the map. The numerous and important faults which traverse the district and determine the contour of the land, have all a north and south strike, or lie a few degrees to the westward. The average distance between them is rather under a mile. Occasionally there are small cross-faults running into the main-faults, but seldom, if ever, crossing them. The direction of both the principal and minor faults is precisely the same as those which intersect the Wigan coal strata, from which it may be assumed that the forces acted in the same direction which produced each series, and also that they were coeval in time. The fractures in the Trias were probably coincident with the upheaval of the strata, and occurred soon after its deposition and consolidation in the Liassic period. When the fissures between the walls of the faults opened, they seem to have been immediately filled with sand from the sea above, and by fragments dislodged from the sides. Often a subsequent extension of the fracture allowed a further infiltration of debris, which has caused the flag-like character observed at the sides of many faults. If, as is very probable, the land was elevated above the sea level at the time the numerous faults originated, the lines of dislocation must have formed long open ravines, and the surface must have been rugged and uneven; such a supposition would satisfactorily account for the enormous denudation which has taken place. The more powerful faults often throw the strata off their continuity to the extent of 700 feet, bringing rocks of various Triassic age into juxtaposition. The great fault throwing up the pebble beds of the Bunter along a line from the Dingle to Kirkdale, is a good example of one of the most important of them. A section through it can be partially examined in a quarry in Netherfield-road, where it is 20 yards wide and filled with a very hard compact sandstone of uncertain fracture. There are many slight dislocations and slips of the strata, which frequently produce those beautifully polished surfaces so common in the neighbourhood. These slickensides usually cover the sides of the great faults, but are more perfect on the exterior of the rock between them. In such cases it is evident that the polished surfaces could not have been caused by the original disruption of the strata, but by slight movements afterwards-long after the faults had been filled with debris. A throw of the strata to a very small extent, acting under immense pressure, seems to have been sufficient to cause the phenomenon. This opinion is confirmed by the occurrence of slickensides, at different angles in slides of the rock within the faults, and also by highly-polished surfaces in very slight slips which displace the strata only a foot or eighteen inches. It is very probable that the coal measures might be reached by boring through some of the lower beds of the Bunter formation where they are brought to the surface by faults. Last year a boring in search of coal was made near Waterloo, in the series nearly one thousand feet higher than the Bunter sandstone nearer Liverpool. It is reported that some years ago similar unsuccessful attempts were made at Bidston, in the valley to the west, still higher in the Keuper series. Such investigations are sometimes of considerable scientific interest. If any individual desires to expend a few thousand pounds in order to obtain correct and indisputable geological sections, it would be of more interest to science to commence with the lower Bunter formation, and at the same time more likely to yield some return for the expense incurred. The Keuper formation in Wirral seems to admit of three clear and distinct subdivisions, viz.: the Red Marl, the Red or upper Keuper sandstone, and the Yellow or lower Keuper sandstone; the latter forms a coarse conglomerate towards its base. These upper and lower sandstones comprise the waterstones of my former paper upon the subject. The best localities for examining the red marl occur at Woodchurchwhere the pseudomorphous crystals of chloride of sodium previously described were found—also along the brook between Irby and Arrow, and to the west of Greasby, and at Irby-hill. The following section, taken between the two last-named places, shows the red marl reposing upon beds of red sandstone, dipping to the east. SECTION AT GREASBY.-QUARTER OF A MILE. W. Keuper Red Sandstone, with Red Marl reposing upon it. E. At Upton, and several other places the marl reposes upon thick beds of red sandstone. There seems to be no outcrop of any underlying strata in that locality, though it is very clearly shown that the red marl rests upon the red or upper Keuper sandstone. The next section deserving particular attention is one through Oxton-hill. There is a road parallel, but a little to the north of the turnpike from Woodchurch to Oxton in which the soft red strata of the upper Bunter crop out to the west. These are probably succeeded by the variegated beds, for on ascending the hill the yellow beds of the same subdivision are seen to crop out from its base. Near the top, the conglomerate, or basement bed of Keuper sandstone is visible. This, the lowest stratum of the formation, is generally indi cated by the presence of a rocky ridge, and by large detached masses rolling down the adjacent slope, from the wearing away of the softer rocks beneath. At the summit of the hill there are two large quarries exposing about 20 feet of the lower Keuper sandstone, the bottom of the bed being a very coarse white conglomerate, the upper part yellow, and terminated by four feet of marl. To the east of the quarries a soft yellow sandstone reposes conformably upon this bed of marl, and may be considered to represent the greater part of the lower subdivision. SECTION AT OXTON HILL.-ONE MILE. W. E. Bunter Sandstone. Keuper Sandstone. This yellow sandstone I have traced over the hill to Christ Church, where it appears to gradually sink under the red or upper Keuper sandstone of which the church is built. There is a new road to the west of that edifice, over the bare rock, where the junction of these yellow and red strata can now be examined. A little to the east a large quarry is open in the beds of red sandstone. They dip S.E. by E. at about 7°, are of coarse texture, light red shade, and contain occasional pebbles, the two visible beds being separated by a band of marl which thins out to the north. At the eastern end of the quarry three or four feet of marl sandstone, no more rock being visible. deep valley containing a thick deposit of Boulder clay; beneath, there are very likely to be some of the lower beds of the red marl, if that shown at the quarry is not the base of it. The character of several bands of flagstone where it joins the rock seems to favour such an opinion. overlie the red Beyond, there is a At Bidston and Flaybrick the same order of succession |