framework, however, was laid by James Richardson during summers of 1857 to 1863. His results were first published by Billings in 1862 but appeared in detail in the "Geology of Canada" (Logan, 1863). Richardson worked almost entirely in west Newfoundland where he constructed a strati graphic section that has remained the basis of all subsequent investigations (Table I). As a result of Richardson's work in west Newfoundland, Logan was able to correlate these rocks with the Quebec and Taconic Groups and conceived his idea that not only was much of the Quebec Group in Quebec and Newfoundland allochthonous, but, prior to its transportation, it formed part of an ancient con- tinental margin (Stevens, 1974). This aspect of Logan's work is treated more fully later in this thesis.
 Following the publication of the "Geology of Canada", the New- foundland government started a geological survey of its own in an attempt to develop the economy of the island. Alexander Murray, previously Logan's assistant in Quebec and Ontario, was hired in 1864 to direct the Survey. A short biography of Murray is given by Bell (1892). In 1869, James P. Howtey became Murray's assistant and eventually succeeded Murray when he retired in 1883. Howtey retired in 1909.
 The results of the Survey are contained in annual reports to the Newfoundland government which were compiled and published in book form in 1881 and 1918. Murray compiled the first geological map of the island in 1873. It was reissued in 1877. Howley published a map in 1909 with reprintings in 1915 and 1925.
 Murray and Howley studied most of the coastal and river sections in west Newfoundland and described them using Richardson's stratigraphic nomenclature. Much of their work concerned the potentially  economic rocks of Carboniferous age but also delineated the distribution of older rocks which they referred to the Cambrian and Silurian systems. (It is hard to understand Shuchert and Dunbar's [1934, p.3] criticism of Murray's assignation of Ordovician rocks as Silurian since at the time Murray started work there was no Ordovician system. Murray was merely using stratigraphic nomenclature used at the time by the Geological Survey of the United Kingdom.)
 The relevant parts of Murray and Howley's reports are those for 1864, 1865, 1866, and 1877. A brief review of the early Newfoundland Survey publications can be found in Nature (A.G., 1876). Even at this early date the significance of geological investigation in Newfoundland for the interpretation of the geology of Scotland appears therefore to have been recognized.
 Although Murray and Howley's work did not lead to any basic change in the understanding of the geology of west Newfoundland it did stimu- late several private economic surveys. Most of the reports of these surveys are in the Newfoundland Government files and are listed in Betts (1936) and Butter and Barttett (1969).
 During the early part of the present century, Yale and Princeton universities established field programs in Newfoundland. The main concern of the Yale group, directed by C. Schuchert, was the sedimentary sequences of west Newfoundland. The Princeton group, directed by G. van Ingen, concentrated in Notre Dame Bay and, later, northern Newfoundland and the Bay of the Islands area.
 The results of the Yale program are contained in Schuchert and Dunbar's (1934) "The Stratigraphy of Western Newfoundland", though several theses were submitted after this date (Sullivan, 1940; Troelsen, 1947; Smith, 1952; and Weitz. 1953).
 The stratigraphic sequence established by Schuchert and Dunbar is reproduced in Table I. According to Schuchert and Dunbar (1934), the Lower Cambrian Labrador Group unconformably overlies Laurentian Gneiss. No Middle Cambrian rocks are present. The Upper Cambrian is represented by the March Point Formation which marks the onset of shallow water carbonate sedimentation that continues from the Canadian (St. George Formation) to the Chazy (Table Head) and the Black River (Long Point).
 The lowest Canadian Green Point Series of graptotite-bearing shales and thinly bedded limestones presented difficulties of inter- pretation since they very much resembled the presumed much younger Humber Arm Series. Schuchert and Dunbar (1934, p. 40) suggested that the Green Point Series was either older than the St. George or a near shore fades of the St. George. They preferred the former interpretation. A spectacular sequence of limestone breccias above the Table Head was taken to have formed during Middle Ordovician thrusting since in at least one locality the breccias are interbedded with Middle Ordovician graptotite-bearing shales. The faulting was thought to be related to uplift in the east that gave rise to the thick clastic sequence of the Humber Arm Series of Mid and perhaps Late Ordovician age. No diagnostic fossils were reported from the Series except from close to its contact with the Table Head.
 The entire Cambro-Ordovician sequence, broken only by dis- conformities in Middle Cambrian time and at the base of the Table Head, was thought to have been deformed at the end of the Ordovician  
Historical Geology of Newfoundland
 we9tera             (No^SamXr)      IntCTior         Southea-ten.
 Pleistocene______ GIadation and crustal oscillation.
 Pliocene to Eocene   No sedimentary record.Peneplane of summit of Long Range uplifted and partially destroyed by long
 ___________   erosion. reducing the Gulf of St. Lawrence area to a lowland later submerged by crostal warping.
 Bjjic us       
 No sedimentary record known. Newfoundland probably subjected to continued erosion.
 Permian_______ Folding and faulting danoff Appalaekutn revolution followed by long erosion interval.__________
 Land interval
 Pennsylvanian       ?L^ g^, Measures. all conti-          ,                  ,          Erosion interral
 ____________ Land interval
 Windsor series of
 ,„ . . .         __ ,                                              Humber River, Windsor dif'
 Miasissippian       Windsor series S450'               No record known    Deer and Grand  turbaw
 lakes, and Bad In- Erosion ioterrai
 .____________ ______________________ ____________ dian Lake_____ ___--_________
 _ Land interval                  Acadian dittw^ww Acadian disturbance
 p Acadian dzstmbsnw sad bwe    and baaic intru-   and basic intro- Acadian du<)'^aie»
 Devonian          __ intrusions___________ aiona________ aions________ _____________
 ^ Clam Bank •erie
 1700'       No record known   No record known   Erosion interval
 Silurian in White                   Sil urian orob
 Silurian            No record known                  No^r^'4? ^d No record known    ably depoai tod. Now
 _______________________________(20W)        y____________eroded away
 _____d»vs^_    disturbance         disturbance          di^^nn     Taconusn ditturbww
 Humber   Arm Present in Piatolet          ,
 5         Q     aeriea at least   Bay in far N. Also „,   . '
 ^ -.   much    5000'            in Notre Dame VOI"""C'.,,
 _,      extended Highland
 rising Bay with B«d Cliff sual€s wlth 8"?"
 g __ _____  toeaat_____ volcanica______ tollte'
 s              Cow Head thruat ••- «
-     v     breccia                            -,      , ,
 "5               Faultinff •ml <•)«.                     No record known   . „         ,
 ^                vation          GOM Pond volcao-   -                 An y°«W,to™»
 OrdoTirian          -3 ^: ——0— ————5————— ica                ,., ,   .——————  tions eroded away
 SS? much  ^"S Ft- ""w                   ^y01?"",
 __ a= exTend^ l5sot         ____________ ^^bly repre-
 1  &•    N    ^ ».. ,T .   .   sno01" Arm vol- Table Head present'
 ff S     to     Fable Head acnes camcs              as  shales with
 -; Q     K     ls80'          Table Head prewat  graptolitw
 ^__________________as shales______^)lcanics____________
 5       I     St. Georm series Laler SL GeorS« Late St. George Wabana 3000'
 -5      n     1570'-3080'+     present aa slates  present with grap- BeU I. 6000'
 g    ——u——________'      with volcanic-       tolites Volcanica  Clarenville_____
 ,=    . Q    Green Pt. series Probably repre- T;~—————~—~——————
 ___________'"'    in port   1700'-f-          3r-'ted             No record known    Pos«tbly represented
 d             March Pt. series                  '''~~~ ~~'~~——————"
 ^   _____  1180'T-                ?                 p         Johanman 400'-500'
 C^ri.n            1_____Land interval               ;                         Manud, 300'
 6      »     Labrador series         ,                           ~r~~.~~~
 .S       »      2600'                  ?                 ?         Hanfordian
 ___________   '~'       A___________ ____________                    Etcheminian 200'
 Proterozoic          Great unconformity                Great unconformity ~——~——-————————-————————-
 ____________Record unknown____________Record unknown    Record unknown   Avalon series 15,000'
 Archeozoic           PLaureutian )?ranite                 ~''— Tu,,^nni-;^» ^. „•«.— "T————-—————-——•
 -———-—————————————————-—————————————____________I J,aurent»an graoite I Laurentian granita
  
during the Taconic orogeny and to be unconformably overlain by the Clam Bank Series of red beds of Lower Devonian age. The Acadian orogeny, accompanied by the intrusion of the ultramafic and mafic Bay of Islands Complex, further deformed the rocks of west Newfoundland which were then eroded and covered by Mississippian and Pennsylvanian sediments de- formed during the Appalachian revolution (Permian age). This geological framework served, with a few exceptions, as a standard frame of re- ference for all workers until 1963.
 Meanwhile, the Princeton geologists Ingerson (1935, 1937), Cooper (1936) and Buddington and Hess (1937) studied the Bay of Is- lands Igneous Complex. Ingerson, working in the northern part of the Complex, concluded that he was examining layered laccoliths of ultra- mafic and mafic rocks, most probably of Lower Devonian age. Buddington and Hess, working in essentially the same area felt that the intrusions were lopotiths. Furthermore, they thought that Table Mountain and North Arm Mountain formed parts of a single lopolith disrupted by westwards thrusting. Cooper (1936) reached a similar conclusion white working in the southern part of the complex. He suggested that the Blow me Down and the Lewis Hi 11s massifs were part of a great disrupted lopolith with a thickness of about 7 miles. He suggested that the floor of the lopolith consisted of schists derived from the Humber Arm sedi- ments and recognized that the roof consisted of volcanic and sedimentary rocks. Cooper (1936. p. 8) considered that the southern part of the Complex consisted of a gravity differentiated body with primary rhythmic banding and a secondary, parallel tectonic banding. Furthermore, Cooper recognized that the Bay of Islands Complex was related to the Mount Albert Complex of the Gaspe Peninsula of Quebec.8 All workers agreed that the igneous rocks intruded the Humber Arm Series.
 Cooper (1937) extended his work to the Hare Bay region of New- foundland under the auspices of the Newfoundland government. Table II shows his stratigraphic column and correlations. The most striking feature of the Hare Bay area recorded by Cooper is the spectactular thrusts that bring the Hare Bay uttramafic rocks and the Goose Cove Schists over the little metamorphosed Mai-den Point and Goose Tickle sediments. Cooper (1937, p. 11) compared the thrusts with the Moine thrust of northwest Scotland. He correlated the uttramafic rocks above the thrust with the Bay of Islands Igneous Complex white the clastic rocks below were thought to be in place and equivalent to the Humber Arm Series of Middle Ordovician and later age.
 Betz (1939), also working from Princeton, described the geology of the Canada Bay area, south of Hare Bay, in terms of Schuchert and Dunbar's standard section. His stratigraphic column and correlation are reproduced in Table III.
 Between 1949 and 1955 several students from Columbia University, mainly directed by Marshall Kay, worked in west Newfoundland. These included walthier (1949). Oxtey (1953), and Nelson (1955). Of particular note is Walthier's suggestion that the metamorphic rocks east of Corner Brook are thrust over the carbonate rocks of the St. George Group. This suggestion, yet to be reconfirmed in the field, implies the existence of a Moine thrust-like feature in west New- foundland.
 The work of the American universities in western Newfoundland 'broadly confirmed and considerably refined the earlier results of the  
 Western Newfoundland             	Hare Bay
  							7. Ireland Point Volcanics
 2,000'
 Humber Arm      			 	6. Maiden Point sandstone
 Series              				6'000’
 5,000’				       		5. Goose Tickle Slate
 2,000'-5,000'

 Cow Head
 Breccia         				4. Northwest Arm Formation
 0-500'

 Long Point
 Series
 1,530'
 
 Table Head      				3. Hare Island Limestone
 Series—1,380'        			1,000'
 
 St. George      				2. Southern Arm Limestone
 Series              				1,500'+/-
 1,570'-2,080'
 
 Green Point     			1. Brent Island Limestone
 Series                 				350'+/-
 1,700’
 
 Table II. Stratigraphic Column and Correlations used by Cooper, 1937.

         Age                  		Betz (1939)
 Lower Middle               		Bide Arm Fm.
 Ordovician
 Middle Cambrian to         	Chimney Arm Fm.
 Early Ordovician
 Middle Cambrian            	Treytown Pond Fm.
 Early Middle               		Cloud Rapids Fm.
 Cambrian                   		
 Lower Cambrian            	Forteau Fm.
 Lower Cambrian             	Devils Cove Fm.
 Table III. Stratigraphic Column used by Betz, 1939.
  
Canadian and Newfoundland Surveys. Logan's broad stratigraphic synthesis was polished, expanded and placed on a more secure basis.
 However, one curious and apparently minor difference of interpretation occurs in the descriptions of the Bonne Bay area given by Logan and a footnote in Schuchert and Dunbar.
 Logan (1863, p. 293) insisted that certain rocks, later included by Schuchert and Dunbar in their Humber Arm Series, were the equivalents of the Sittery and Levis Formations of his Quebec Group in Quebec. Logan's view was based mainly on lithic similarity and apparent stratigraphic position. Schuchert and Dunbar disagree (1934, p.95 ) ... in this correlation, however, Logan appears to be wrong, since the greenish sandstones of Bonne Bay are not of Lower Ordovician age but are now known to be younger than the Long Point (=B1ack River) time.
 The key to much of the present interpretation of the geology of west Newfoundland is hidden within this apparently minor difference of opinion. To appreciate its significance, it is necessary to review briefly the early history of the Taconic problem in west Newfoundland, Quebec and New England. More detail can be found in Stevens (1974) and Zastow (1975).
 Early workers in the New England states and Quebec recognized three major rock sequences. The oldest rocks, gneisses and granites, formed the basement and the western foreland of the Appalachian system. These were referred to as the Laurentian System. The overlying rocks, sandstones, shales and carbonates of Cambrian and Lower Silurian (Ordovician) age, were subdivided into the Potsdam Group, the Calciferous, Chazy, Trenton, Hudson River, and Utica Formations. The third sequence of rocks, the Quebec and the probably correlative Taconic Groups, consisted mainly of clastic rocks. These were virtually without fossils and of intransigent aspect. They "looked" older than the second group and this was indeed Logan's first hypothesis (Logan, 1863, p. vii). Later field work demonstrated that in fact the Quebec Group rested on the fossiliferous Hudson River Formation. Logan assumed this was a normal sedimentary succession. Fossils were discovered in the Quebec Group and by 1860 '-' paleon- totogical evidence enabled Billings to state that the Quebec Group fossils were older than the Utica and about the same age as the under- lying Calciferous and Chazy Formations. Logan's first reaction was to believe the field data and to suggest that colonies (in the sense of Barrande) of older fossils had survived into post Utica times (Logan, 1860, in a tetter to Barrande, quoted in Logan, 1863, p. viii). In the same year, after more fossils had been collected, Logan realized that the doctrine of colonies could not explain the exclusively primordal aspect of the fauna. He was forced to conclude that parts, at least, of the Quebec Group were time equivalents of the Calciferous and Chazy Formations. Now the problem was how could the Quebec Group overlie its time equivalents? Logan concluded that the Quebec Group must have been transported. He suggested that a great dislocation at the base of the Quebec Group brought it over the Utica Formation. Logan explained the lithological differences between the two sequences by suggesting that the autochthonous sequence was a shallow water shelf sequence whereas the Quebec Group formed in deep water at a con- tinental margin. The ocean was named the Paleo Atlantic (Stevens, 1974, Fig. 3 ). It is not clear if this name was ever used by Logan or if it was coined by Dawson (VD_ Harrington, 1883).
 Logan, on the basis of Richardson's observations, recognized that the "Great Dislocation" should pass through the Bonne Bay area of west Newfoundland between his divisions N and Q. Logan, in other words, recognized that the Humber Arm Supergroup was transported. Schuchert and Dunbar rejected Logan's correlation and it was a hundred years before Logan's hypothesis was fully substantiated.
 Schuchert and Dunbar's failure is difficult to understand since, in the Taconic region, Ruedemam (1909) and Keith (1913) recognized that the Hudson River Group was thrust into its present position.
 This hypothesis was neither fully accepted or conclusively proven until quite recently (Zen, 1961), and several rival hypotheses existed (Zen, 1967). It is possible, therefore, that Schuchert, who started work in Newfoundland in 1910, did not accept the Taconic Klippe. However, Schuchert (1930, p. 711) shows that he understood the regional significance of Ruedemann's work and its relationship to Logan's work. He appreciated that Logan's Line "may be traced from Kingston, New York, and Lake Champlain to Quebec City, and thence it follows the estuary of the St. Lawrence, undoubtedly continuing to the south of Anticosti." (Schuchert, 1930. p. 711). Furthermore Schuchert realized that the thrusting took place within.the Ordovician Period (Schuchert, 1930, p. 718).
 In Newfoundland, Schuchert and Dunbar (1934) and Dunbar (1934) recognized the importance of Middle Ordovician thrust faulting and found an anomalous sequence of rocks, the Green Point Series, indistinguishable from the Humber Arm Series (Schuchert and Dunbar, 1934, p. 38). Even with their wide knowledge of Appalachian geology, and the field evidence (the thrusts are clearly visible at several localities), Schuchert and Dunbar failed to make the logical deduction that the Humber Arm Series was, in large part, transported. Indeed. Schuchert (1930, p. 712) says "... the Quebec Group . . . (is) known in situ only in western Vermont and northern Newfoundland.". Perhaps part of the failure is explained by the scarcity of fossils in the Humber Arm. The fossiliferous Cow Head Breccias were misinterpreted as tectonic breccias and the fossiliferous Green Point Series was assigned an autochthonous position beneath the St. George even though it is never seen in this position.
 Perhaps of even greater importance is the marked fades convergence between the transported Humber Arm and the top of the autochthonous sequence. This is explained in a later section and it is sufficient to note here that the richly fossiliferous rocks above the Lower Table Head greatly resemble those of the Humber Arm, and it would seem logical, therefore, to assign a Middle Ordovician or later date to the Series.
 In 1941, however, H. Johnson, who had been working for the New- foundland government, recognized that the anomalous Green Point Series was only the oldest member of a thick sequence of shales, sandstones, carbonates and carbonate breccias, coeval with the St. George and Table Head Formations, that is of Tremadoc to Llanvirn age. Johnson (1941) separated the anomalous rocks from the unfossiliferous main bulk of the Humber Arm. He erected three new groups, the St. Pauls Group, the Western Brook Pond Group, and the Green Point Group. Johnson realized that his three new groups could not be fitted into Schuchert and Dunbar's