All three curves thin out between 1100 and than the loeal glaciers (after H. Ahlmann). 1700 metres above sea level. This indicates that the height of the Inland ice and the Another and more possible eause for the fast julianehäb ice cap must have been rather thinning out of the lowermost eurve eould constant through most of the holocene pe­ be a new wave of iee indicating a future riod, It is in aceordanee with the theoretical advance. Push moraines in high er altitudes considerations of the plasticity of an iee of thc Qoroq and Kiagtut sermia glaeiers eap, as given by ]. Orowan and ]. Nye. eould be so interpreted. Considering this It must be noticed, thar the trim line thins mechanism, we should have a melting and out ca. 1200 metres above sea level. One retreating system in the lowermost parts of factor eould be that the Inland Ice and the the lobes From the iee eap, but an expand­ julianehäb ice eap, expressed as a function ing system of ice in the areas near the firn of the altitude, than have an ablation less limit.

Glacial Geology of Northern Greenland * William E. Davies, Washington ,:-,:-)

Abstract. From 1950 through 1900 studies on the Sinee 1956 the D.S. Air Force Cambridge glacial geology of northern Greenland have been made in co operation with the U. S. Air Research Laboratories has condueted studies Force Cambrf.dge Research Laboratories. As a result of these studies foul' distinct phases of of landforms and enginering properties of the latest glaciation have been recogrrizcd. The soils in northern Greenland. Members of last glaciation extended over most of the land and removed traces of previous anes. Retreat the U. S. Geologieal Survey participated in of the ice mass began some time previous to 0000 years ago. This was followed by a rtse in the geological aspcet of this research, and sea level which deposited elay-silt sueeeeded by investigated the glacial geology of Peary karne gravels around stagnant ice lobes in the large valleys. Marine terraees, up to 129 meters Land, Kronprins Christian Land, and ad­ above present sea level, developed as readjust­ jacent areas. ment occurred in the land free of ice. About 3700 years ago an advance of glaciers down major fjords took place followed by retreat to Northern Greenland consists of three major approximately the present position of the Ice. physiographie divisions: Till in Peary Land, north of Frederick E. Hyde Fjord, contains only Iocally derived matertals indicating that the central Greenland ice cap 1) an area of low alpine mountains in did not cover the area. Pcary Land, north of Frederick E. Hyde Fjord, Zusammenfassung: Glazialgeologie von Nord­ 2) similar mountains along the northeast grönland. Von 1955 bis 1900 wurden in Zusammen­ arbeit mit den U.S. Air Force Cambridge Researcll coast south of Independence Fjord, and Laboratories Studien über die Glaziaigeologie von Nordgrönland gemacht. Als ein Ergebnis dieser 3) a dissected plateau formed of non-Iol­ Untersuchungen wurden vier getrennte Phasen ded late Preeambrian and early Paleo­ der letzten Vereisung erkannt. Die letzte Ver­ eisung dehnte sich über den größten Teil des zioc rocks inland from the mountainous Landes aus und beseitigte Spuren von vorher­ gegangenen. Der Rückzug des Eises begann vor eoastal areas. gut 6000 Jahren. Dieses wurde aus dem Anstieg des Meeresspiegels festgestellt, wobei Ton und The glacial geology of northern Greenland Schluff gefolgt von Kame Schottern rund um has been given scant attcntion. Lauge Koch die stagnierenden Gletscherzungen in den gro­ ßen Tälern abgelagert wurden. lVlarine Teras­ outlined the basie concepts of former gla­ sen - bis zu 129 m über dem jetzigen Meeres­ spiegel - zeigen, wie der Rückzug in dem eis­ ciation, which wcre based on observations freien Land eintrat. Vor etwa 3700 .Jahren fand made while on the Danish Bicentenary ]u­ ein Vorrücken der Gletscher durch die I-Iaupt­ fjorde statt, gefolgt von einem Rückzug auf bilee Expedition in 1921 (Koch, 1927, etwa den gegenwätttgen Eisstand. Grundmorä• nen in Peary-Land, nördlich des Frederick E. 1928a, b). Troelson (1949, 1952), while on Hyde-Fjordes, enthalten nur örtliches Material, ehe Dansk Pearyland-Ekspcdition 1947-50, was beweist, daß das zentrale grönländische In­ landeis dieses Gebiet nicht bedeckte. filled in details around Brerilund Fjord.

*) Publication authorized by Di rector', U. S. Geological Survey **) William E. Davies, U.S Geological Survey, Washington 25, D.C., USA

94 Eigil Knuth, on his traverse of Danmark gray, poorly-bedded, and generally contains Fjord in 1955 (Knuth, 1958), collected in­ large quantities of pelecypod shells, The forrnation concerning marine terraces. Field­ maximum height of the deposits is 105 me­ work for the present paper was done during ters on Polaris Promontory in northwest rhe summers of 1956,1957,1958, and 1960. Greenland, whereas elsewhere in northern Greenland the height varies greatly. Along Features o} Glaciation Danmark Fjord the maximum height rises Foul' major types of deposits, rnoraines, from 24 meters at the head of the fjord to clay-silt, kames, and marine terraces, reflect 41 meters midway along the fjord in a di­ more extensive glaciation in the past, These stance of 90 km. This gradient, 0,45 meter Features occur throughout all of northern per kilometer, is 10 times as great as that Greenland but they are best developed of the tilt of the younger raised marine ter­ along, and south of, Independence Fjord. races that have been formed on the clay­ e 1 a y - s i 1 t D e pos i t S- Deposits of silt. Along the coastal areas of Peary Land clay-silt occur along may of the fjords and the gradient appears to be reversed. At river valleys of northern Greenland, as weIl Bronlund Fjord the maximum height of the as on portions of the narrow coastal plain marine clay-silt is 68.6 meters. Eastward bordering the mouritains on the north side and northward along the coast of Peary of Peary Land (figure 1). These deposits Land it declines in altitud- until along the have two origins, lacustrine and marine; coast west of Kaffeklubben 0 and on and along the lower part of river valleys in Kaffeklubben 0 it is only 2 meters above coastal areas they grade from one type to present sea level. In most of this area the another in short distances, clay-silt is covered by later terrace gravel. The marine clay-silt occurs throughout most The pelecypod fauna in the marine clay-silt of northern Greenland and is uniformly beds is uniform throughout North Green-

40 20

KAP MOIlR:l$ Jf$UP ~V'-'"",k

82

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/' c E

'00, Figure 1: North Greenland, clay-silt deposits. Marine deposits shown by vertical !ines, lacustrine deposits by horizontal lines, aeo!ian deposits by dots. 95 land and is characterized by an abundance inland 70 km to an altitude of 200 meters. of H i a tell aar c t i c a (Linne) and In these areas the clay-silt has been greatly M y a t run c a t a Linnc. A few gastro­ eroded by wind action, and the deposits pods are also present. form low rounded hills 'wirh dunes deve­ Lacustrine clay-silt deposits are extensive loped on broad, flat areas. south of Independence Fjord and occur M 0 r a i n e san d Kam e s Three over much of the large valleys between groups of moraines developed during the Centrum So, Ingolf Fjord, and Hekla Sund, latest glaciation occur in northern Green­ and in the long parallel valleys west of land. The oldest moraines, antedating Danmark Fjord. They are generally over­ clay-silr deposition, liealong the coastal hin hy kame terrace deposits; but in an plain on Herlufsholm Strand and on the area 15 km long and 5 km wide east of north coast between Frederick E. Hyde Centrum So, the clay-silt is at the surface. Fjord and Kap Morris Jesup (figure 3). A Maximum height of the clay-silt in tbe large morainal system on the northeast side area of Centrum So is 137. meters above of Independence Fjord opposite Danmark sea level, 37 meters above the level of Cen­ Fjord is probably of the same age. trum 50. Topography of the clay-silt where The moraines on Herlufsholm Strand luve not covered by kame deposits is typically been modified by a marine invasion that "Badlands" with relief of 10 to 30 meters, planed and covered them with aveneer of The lacustrinedeposits are thinly bedded gravel but a few of the larger ridges still and appear to be varves (figure 2). No fos­ are readily distinguishable: One ridge ex­ sils have been found inthe lacustrine bcds. tends northwest along the central part of In the valleys west of Danmark Fjordand the Strand, while the others are close to near the .icc cap west of Centrum So rhe the mountains. Iacustrine clay-silt beds are as much as 36 On the coastal plain northwcstof Frcderick meters above the valley floor, and extend E. Hyde Fjord marine planation has remo-

Figure 2: Lacustrlne ctay-süt 1 mile east of Centrum 80 showlng varveIike beddrng. 96 - MAJOR: MORAlNE Figure 3: North Greenland, major moratnes ved most of the old moraine. In this area few erratics, and old moraines are eonfined the plain above 110 meters is formed of to the side of the river valley, bedrock with little or no moraine exeept at The largestand most extensive system of the mouth ofFrederiek E. Hyde.. Fjord old moraines in Peary Land is on the north where later moraines oeeur. Below 110 me­ side of Independenee Fjord opposite Dan­ ters the plain is formed of strands of beach mark Fjord. Thisarea, 600 square km, is gravel. Old moraines from a glaeier For­ made up of a complex of morainal ridges merly extending into Bliss Bugt, southeast and intervening outwash plains. The rnajor of Kaffeklubben 0, form irregular gravel moraines on the north side trend east-west; ridges as weIl as 3 parallel groups of islands in the rest of thearea they trend north­ along the eoast 40 km northwesr of Frede­ south. The highest moraine is the northern­ riek E. Hyde Fjord. most one; at its eastern end, 6 km north of On the coastal plain south of Kaffeklub­ Independenee Fjord, it reaehes an altitude ben ° old moraines are larger .and more of 150 meters (figure 4). The top of this numerous than elsewhere along the Areeie moraine consists of a seriesof peaks sepa­ coast of Peary Land. Three large moraines ratcd by narrow saddles, Up to 106 meters are parallel to the eoast and mountain front; altitude the moraine eonsists of gray boul­ a fourth moraine forms a seriesof low is­ der day; above this it is mainly boulder lands and shoals several kilometers offshore. cobble moraine with sand. North of the mo­ Kaffeklubben '" is the most prominent part raine is a broad area of outwash, The smal­ of these moraines. West of this area no ler moraines to the southform irregular; prominent moraines exist and the rock plat­ lowrounded ridges and are mainly cobble formalong the coast rises rapidly in alti­ grave1 with . clay and boulders. Marine tude, At Kap Morris Jesup the platform shells oceur in these moraines within 4 km is formed of frost-rived bedrock with very of the eoast indieating the moraine was

97 Figure 4: Major moraine, 6 km north of Independence Fjord opposite Danmark Fjord. Lower part (light color) is cobbly ciay; upper part is gravel. probably deposited in shallow coastal seas. large valleys extending north and south Moraines younger than the clay-silt deposits from the fjord. are not eommon in North Greenland. In the Kame areas coineide closely with the distri­ area between Centrum S0 and the ice eap bution of laeustrine clay-silt (figure 5). In 6 morainal ridges are developed on the rhe large interconneeting valleys south of upland surface. These moraines end in Ingolf Fjord, west of Danmark Fjord, east marginal ehanne1s and terraces in the val­ of Midsommer S0er, and at the head of leys. Similar upland moraines oeeur on the Danmark Fjord kame terraces with large plateau north of the lake. lakes cover most of the valley floors. The surfaees of the terraees are smooih with Along Hekla Sund moraines lie above the little discernible slope, They are formed of clay-silt beds at the mouths of large river rounded pebbles and cobbles a meter to over valleys. Along the northern part of the 30 meters thick, generally lying on clay-silt, sound these moraines are only a few meters The lakes are in steep-sided kettles exten­ above sea level while to the south they are ding into the clay-silt. as mueh as 118 meters above present sea level. They are probably related to an '1d­ Marine Terraees Throughout vance of a tongue of the Nioghalvfjerds­ northern Greenland raised marine terraees fjorden north along Hekla Sund. arc eommon (figure 5). The best developed terraces are at the mouths of major strearns Other moraines of similar age are in the where delta terraces oeeur. Here, deltaie tributary valleys of the rivers draining to material is planed and reworked as the sea Hekla Sund and on the eastern side of level is lowered relative to former positions J. C. Christensen Land. of land (figure 6). The terraees are well­ developed but are limited to the small areas Reeent moraines have been built up at the of the delta. This type of development is front of many valley glaeiers. The most typical on rivers entering Hekla Sund, In­ prominent are along Ingolf Fjord and the dependenee Fjord, and Danmark Fjord.

98 40 20

82

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100,

- KAME TERRACE :.:.: MARINE TERRACE Figure 5: North Greenland, distribution of kame and marine terraces

Figure 6: Delta terraces, east side Danmark Fjord, 45 km from south end. Delta beds are deposited on marine clay. 99 Marine terraces also occur along the broad terials along a rising coast; and they extend coastal lowlands on the north coast of for greater distances, but are less developed, Peary Land and along Independence Fjord. than the delta terraces. In contrast to the delta terraces, these Most of the marine terraces contain deposits beaches are developed by reworking of ma- of gravel with a matrix of fine to coarse

IV ". 0­ 0> e o e o s , I 1 L-__-'-- I I m , }>­ , RIVIERADAL Ul , ~I -i , , I -~-~'''--_.- ,, ,: .: SAEFAXI ELV () " . o : : , , , ,i HEKLA SUND }>­ , , " , , -----~rr- INGOLF FJORD Ul , ' , , 1 ' , , -i 1 , ' , , , : , SOUTH BRANCH . HEAD OF : I DANMARK FJOR{) /111 11 1 : I 1,'1"" ,1 KAP VIBORG 1I I:: I: : , · · KAP RENAISSANCE .." · , . ;;0<5 , o , NORD , 1 , , HEAD OF 'I" , BR(2lNLUND FJORD z o " " . MOUTH OF m 1'Dr~1: BRi2lNLUND FJORD :;: ;;; ?: ." » » m I x z Z 0 (; o K0LEN ~ :oe :oe m ~~l_I C 1III I I ~ :;:. ~ Z () NEAR FALKEFJELD » » m ~ :oe :oe I TROElSEN 1952 ::! Z Z , , I .... m m , I' I C I , KAP PETER HENRIK 0 ...... , ," , , m m m , I , :oe'" :oe " Q » »'" (;l (;l --r KAP RASMUSSEN n I ); 111 -< ill " KAP WYCKOFF VI 'I' " I ~ , " , z , , 10 KM ·SOUTH m 1 I1 TI_U1~ OF SKAGAN '"0 o i ______. VI ~ 111 11 . :I: III I' : SKAGEN "I iI : . () " , I , o I' , }>­ I' I I : DEPOT BUGT 1 Ul I I , -i " rD 1= ." KAP OLE CHIEWITZ m I; I1 }>­ ;;0 ." I , :u I -< .11 J I KAFfEKLUBBEN i2l ,.. .11 , I 1 1 }>­ , , , Z I I JIII , DOBBELTS0 o I 1 " 1 " 1 1

::::::: KAP MORRIS JESUP 11 11::::,I :'l'Ii"IIi" 1 POLARIS PROMONiORY I, ,,," 1 · NORTHWEST GREENlAND Figure 7: Major te rraces, North Greenland. 25-37, 45-57 terrace accentuated by heavy line. 100 sand. Subroundet to rounded pebbles and cut into the clay and are clearly younger cobbles as much as 10 cm in size are com­ than it, mon, The deposits are derived mainly from reworked morainal material and, except Com position of Glacial Till along the north coast of Peary Land, are Independence Fjord and the southern part composed of many different rocks. of Peary Land demarcate the boundary bet­ Tertace development is not uniform at a11 ween two distinct types of glacial till. South points and the number of terraee levels pre­ of a line 33 km north of Independence sent varies from point to point. However, Fjord (Troelsen, 1952) and extending east­ throughout northern Greenland one group ward to a point opposite Danmark Fjord, of terraces is persistent. South of Indepen­ the till contains a heterogeneous assemblage denc- Fjord ir is from 25 to 37 rneters of metamorphic, igneous, and sedimentary above present sea level and north of the rocks of late Precambrian and early Paleo­ fjord, 45 to 57 rneter (figure 7). zoic age (table 1). Included in this type are large quantities of unique pink granite with The higest distincr beach is 127 to 129 me­ prominent angular quartz particles, and only ters above sea level, and is along the middle sma11 quantities of dark minerals. The gra­ part of Independence Fjord and near the nite is similar to that which craps out on mouth of Frederick E. Hyde Fjord. Below the north side of Parker Snow Bugt south this level at least 16 terraces are recogni­ of Thule, Northwest Greenland. This hete­ zahle although a11 are not present at one rogeneous .till, characterized by the pink locality, granite pebbles, is eommon From Thuje In addition to marine terraces, weli-deve­ north through Nyeboe Land and extends loped storm ridges along raised strand lines west into eastern Ellesmere Island near occur below an altitude of 17 meters. On Alert (R. L. Christie, oral communicarion) Herlufsholm Strand 11 we11-defined storrn and east throughout the area south of In­ ridges ean bedistinguished; near G.B. Schley dependenee Fjord. Fjord 14 to 19 are reeognizable; and at the head and the mouth of Danmark Fjord, 18. North of the line 33 km north of Indepen­ dence Fjord, ti11 components vary From The overall tilt of the terraces is towards point to point, but at a11 points the till is the south, However, a secondary tilt is su­ formed of locally derivcd material. The perimposed, and 10ea11y the terraces along characteristic pink granite pebble is lacking Danmark and Independence Fjords are til­ in the northern till. red toward the junction of these fjords. The tilt in the southern part of Danmark Fjord Glacial History is to the south at 0.05 meter/km; in the nor­ In northern Greenland only one glaciation thern part it is to the northeast of 0.015 is recognizable. This glaciation, much of meter/km. which still exists, erased evidence of former Some radiocarbon dating of shells from glaciation. During niaxi111U111 development wirhin the main terraces have been made, of this glaciation the central ice cap of and more are being made. From the data Greenland transported rill charaeterized by on hand, the beaches above an altitude of pink granite pebbles. This glaciation exten­ 24 to 50 meters are between 3700 and 6100 ded 33 km north of Independenee Fjord years old, Those below this level are 500 where it was buffered by loeal ice eaps to 3700 years old. This subdivision is based From rhe high mountain areas along the on dating of the prominent terraces in the south side of Frederiek E. Hyde Fjord. Till 24- to 50-metet zone 'c) as 3780±300 years, laeking the distinctive pink granite pebbles and the lowest strand above present high and with only locally-derived materials is tide as 500 years. The maximum date of eharaeteristies of the glaeial depositsof the 6100±300 )'ears is from the marine day. mountain iee caps. Move111ent of the ice Whete day is present, marine terraces are eap along the north side of the eentral iee

*) Radiocarbon dating by Meyer Rubin, U, S. Geological Survey 101 Tcble I COMPOSITION OF TILL NORTH GREENLAND LOCALITY (percent present) I i ,;: ~ Q) I 'ö '0:: o I .::'" .:: .:: 0 Q) Q) C 'I-f "2 P< sP< P:: "0 Q 0. ;,:~ 0. bJl C

Thule red I I I 3 sandstone & quartzite 30 5 140 15 15 15 50 5 40 I 130 1 I 1 Thule withe I ' ! sandstone & quartzite I 20 I 50 520 15 40 40 20 15 40 40 1 Red Carboniferous i I I sandstone I 25 Gray sandstone I I 20 5 20 I I White coarse sandstone 5 I I Brown sandstone I I I 5 P Black sandstone I 20 Black slaty shale 5 I P

Limestone I 5 15' I 30 30 15 90 25 5 ' 50 5 Basalt I 10 Amphibolite I Felsite 5 I 5 Andesite-black 40 Red porphyritic I 50 andesite I Pink granite PI 10 P 5 P 10 10 PP D iabase 20 30 15 20 20 15 1 5 4 P 30 30 I Red granite gneiss 2 30 Gray gneiss 20 I P 5 5 P 20 2 10 5 I , Chlorite schist I P 40 2 P 20 10 70 20 ! White quartzite 5 85 P I 20 B rown-gray I q uartzite 75 B uff, columnar q uartzite I 5 30 I I Dark purpIe q uartzite P 15 10 P M arble 10 P 10 Gray phyllite 5 S late 5 10 5 G reenstone P I Quartz pebbles 20 5 1 I, I I 102 cap was eastward and northeastward down Afterdeposition of silt and kame materials the troughs of Independence and Danmark the lag in isostatic readjustment resulted in Fjords and other major fjords; movement an inundation of the land which was equi­ along Frederick E. Hyde Fjord was east­ valent to a rise in sea level of as much as ward. North of Frederick E. Hyde Fjord 129 meters along the Arctic coast of Peary and along Herlufsholm Strand glaciation Land. With readjustment, as the land was of an alpine type with valley glaciers emerged, distinet marine terraces developed extending onto and across the flat coastal in coastal areas, plain, South of Kaffeklubben 0 valley gla­ ciers formed a piedmont ice sheet covering An advance of ice, primarily by glaciers the coastal plain. 'I'his piedmont glacier afloat in major fjords, occurred about 3700 was probably similar in form to the shelf years ago. This advance was about 30 to ice on the north side of Ellesmere Island. 60 km down Fjord, and disrupted the tcr­ race forming stage just prior to the Forma­ Abour 6000 years ago an abrupt change oc­ tion of terraces in the zone 24 to 50 meters curred, and a relatively rapid retreat of the above present sea level. Since that time re­ iee took pIace. The ice caps shrunk to about treat occurred until 500 years ago, after their present size and the major fjords and which only minor readjustments in the po­ valleys were occupied by stagnating rem­ sition of the glacier fronts have occured. nants of the former ice sheet. Contempora­ neously with the melting, large quantities of silt were deposited in the open portions References K 0 c h , Lauge, 1927, Report on the Danish Bi­ of fjords and along valley floors, Increased centenary Jubilee Expedition, north of Green­ melting culminated in the resorting and de­ land 1920-23: Medd, om Grünland, bd. 70, nr. 1, p. 50-148. positing of kame terrace materials overlying -, 1928, The physiography of North Greenland; the silt. Isolated remnants of buried ice in Greenland: Comm. for the Direction Geol. and Geog1'. Investigations in Greenland, v. 1, blocks eventually melted and formed lakes p. 514-518. along the major valleys. -, 1928, Contributions to glaciology of North Greenland: Medd. om Grünland, bd. 65-II, p. North of Frederick E. Hyde Fjord the val­ 302-322, 376-382. K n u t h , Eigil, 1958, Det mystiske X i Dan­ ley glaciers and piedmont ice melted back, mark Fjord: Ejnar Munksgaards Forlag, Kü• with most of the outwash material carried benhavn, 40 p. TI' 0 e l s c n , J. C., 1949, Contributions to the off to sea. geology of the area round .rorgen Bronlunds Fjord, Peary Land, North Greenland: Medd. At the point of maximum rctreat the main om Grünland, bd. 149, nr. 2, p. 19-22. ice cap and outlet glaciers were as much as -, 1952, Notes on the Pleistocene geologyof peary Land, North Greenland: Medd. fra 60 km inland from their present position. Dansk Geol. Forening, bd. 12, p. 211-220.

Die Polarlichtzone der Südhalbkugel * Von Otto Schneider, Buenos Aires ,:.,:.

Zusammenfassung: Nach einer kurzen Einlei­ nlschcn Beobachtungen ergaben. Mit der ab­ tung über die Schwierigkeit der Bestimmung der schließenden Bemerkung, daß die Sücllichtzone Lage der Polarlichtzone auf der Südhalbkugel nur Über die I-Iälfte ihres Umfanges einiger­ behandelt der Verfasser methodische Fragen m aßen sicher festgelegt ist, beendet der Ver­ über die Möglichkeit der Definition der Polar­ fasser seine Darlegungen, denen er e lrie Tabelle lichtzone sowie Über die zeitliche Veränderlich• Über d ie I<:oorclinaten der crwähnten Stationen keit, Inhomogenitäten der Beobachtungen und und ein ausführliches Literatur-Verzeichnis an­ über die F'orrn der Zone. Bei den Lösungsver• f'ügt. suchen werden zunächst die älteren Vorschläge, sodann die Isochasmen nach Hultqvist, ferner Abstractr The Polar Light Zone of the Southern andere theoretisch abgeleitete Südlichtzonen so­ Hemisphere. After a short introduction dealing w ie die neuesten Versuche von Bond und Jacka wtth the difficulties of the determination of the dargelegt, die Zone mit Hilfe von wirklichen position of the polar light zone on the Southern Südlicht-Beobachtungen festzulegen. Danach fol­ Hemisphere the author treats methodical que­ gen einige zusätzliche Ergebnisse~ die sich auf st.ions of the possibility of the definition of the Grund der japanischen, britischen und argenti- polar light zone as weH as of the temporal

0) Contribuci6n deI Instituto Antiirtico Argentino NI'. 55. **) Dr. otto Schneider, Instituto Antiirtico Argentino, Buenos Aires, Cerrito 1248. 103