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Here are two plates from Guizhou province. They should be Protrachyceras sp. ammonites from late Triassic. First one: Second front: Second back:

A mini fossil museum exists within the lobby of the Park Hyatt in Chicago, just off Michigan Avenue. I'm guessing not too many people know about it unless they're guests at the hotel. It's a wonderful display of very large Moroccan trilobites, ammonites and various other fossils from around the world. It is free, of course, because it's in the lobby and a nice diversion if you're ever in the area. Another added bonus is it's open 24 hours.

Yesterday I washed my finds found on my last Friday trip and from a trip in spring. The weather in June was very rainy this year. So this trip on friday was the third one this year. I was lucky to find a new Lower Carnian (Julian) and Upper Carnian(Tuvalian) spot on this trip. At my trip in spring this year a wonderfull big Ladinian Protrachyceras archelaus was found. Because I was the whole day in good mood for prospecting I took no pics from the locations and landscape. Today I am a little bit sorry about this because it was a beautiful mountain day truly worth to share with others.

Today I finished prepwork done during wintertime. Three bigger multiplates with Ladinian ammonoids and some smaller ones of Ladinian, Carnian and Norian age. Now the field season 2016 can start.

Disparities in the General differences between Nautiloids and Ammonoids Thanks to the amount of money I had to spend recently to keep my two cars running and my Lady bravely taking care of her ill Mother in Ohio, I am unable to do any field work, at least till I get paid again. I am trying to come up with things to keep busy. I started doing some additional research on my favorite fossils Nautiloids. One of the main problems that occur in some specimen found in the ages between the Devonian and the Cretaceous is how to tell the difference between Nautiloids and Ammonoids since they sometimes have the same general shape. The three most commonly used features to tell them apart, (fig. 1), are septal curvature (Fig.2), simple vs. complex septa, (the wall in between the chambers), (Fig. 3), and the location of the Siphuncle, (the tube that goes through the septa and connects the chambers), (Figs. 4 & 5). I have two nautiloid genus from the lower Mississippian that not only are from the same age but can be found in the same outcrop that do not conform to these general differences. The first nautiloid is Subclymenia in the family Trigonoceratidae. Subclymenia does not have the typical simple suture that nautiloids have owing to the name clymenia (Devonian Ammonoid), (Figs. 6, 7 & 8). Later nautiloids in the Mesozoic and Cenozoic also do not have a simple suture. However, the siphuncle in Subcylmenia is very prominently shown in the middle of the septal wall as is the typical nautiloid (fig. 9). The other nautiloid, genus Solenochellus, that displays a difference also includes these difference with a number of genus under the Super family, Aipocerataceae. The genus Solenochellus does display the typical simple suture of nautiloids but the siphuncle is found on the outer ventral portion of the shell as found in Ammonoids (Fig. 10, 11, 12 & 13) . Well this took care of the majority of this week, now I have to figure out what to do next week.

Last saturday I started my first trip this year. It was a good feeling to be in field again but there is still pretty much snow at higher regions. I was lucky and found a block filled with Triassic ammonoids. The age of the fauna is Upper Triassic, Tuvalian and the small grown ammonoids split out well from limestone. Kind regards Andreas

Season closing Yesterday my buddy and I did our probably last trip for this year. Snow was lying in the clearings around our location but the location we went to was free of snow. All in all it was a good year. We made about 15 trips found lots of good ammonoids and 3 new locations too. The last trip was successful too. We found Ladinian ammonoids in excellent preservation but it was hard work to get them out. Kind regards Andreas

Dear Fossil Forum members! This report deals with ammonoids from the former zone of Protrachyceras archelaus, which is our present Longobardian within the Ladinian stage of the marine Triassic timescale. Fig.1 A beautiful view of the surging “rock waves” of the incoming tectonic thrust sheets. The valley between the two Mountains in the middle of the picture marks the tectonic border between the mainly Triassic Hallstatt Unit and the Tirolikum Unit of the Totengebirgs nappe (in the background). History Since the beginning of the geological research within the Northern Calcareous Alps of Austria in the middle of the 19th century, about 500 species of Triassic ammonoids have been described in great Monographs by Mojsisovics, Hauer, Diener and other early authors. The ammonoids described therein came from upper Anisian to uppermost Norian aged parts of the Hallstatt limestone in Austria. Only in the lower to middle Ladinian period, a gap exists in the rich ammonoid record of these early researchers. This gap was explained by them as an interruption of sedimentation in the Ladinian time or tectonically reduced Ladinian strata during the genesis of the Alps. During these early days no one thought of a collecting gap because Ladinian ammonoid faunae were well described and known from several localities in the Southern Alps and the Bakony Mountains in Hungary. In 1882 Mojsisovics pictured ammonoids of Anisian and Ladinian age in his monographic work “Die Cephalopoden der mediterranen Triasprovinz”. The locations mentioned therein reach from the upper Anisian Schreyeralm limestone here in Austria to several Ladinian locations of the former Austrian provinces Südtirol, Lombardy and the kingdom of Hungary, which were also part of the former Austrian-Hungarian Monarchy at this time. Included in this work were also Scythian and Anisian ammonoids from Croatia and Bosnia-Herzegovina. Fig.2 Frontpage of Mojsisovics second great monograph from the year 1882. “The detailed accurate descriptions and illustrations provided by Mojsisovics are unquestionably the greatest contribution by a single author towards appreciating the astonishing beauty and variety of Triassic ammonoids” (cit. E. T. TOZER). Therefore every recent Triassic ammonoid researcher includes these old works in the standard literature of Triassic ammonoids. These old works were so to speak, a cornerstone for building the marine middle and upper Triassic timescale of our days. Unfortunately the early stratigraphic scales of Mojsisovics had some mistakes. Originally the stratigraphic position of the “Norian” stage was set by him below the Carnian. He used the term Norian for the time frame we today call Ladinian. Mojs. thought that most parts of today’s real Norian Hallstatt limestone of Austria were of the same age as real Ladinian strata in the Southern Alps. Some misinterpret location data, i.e. the wrong assumed position of the fineclastic Zlambach marls as base of the Hallstatt limestone led him to this wrong assumption. It was the Austrian geologist Alexander Bittner, a contemporary of Mojsisovics, who introduced the term Ladinian into literature by recognizing the false assumptions of Mojsisovics. The name Ladinian was chosen by Bittner after the Ladinian folk of the Southern Alps/Dolomites. At this time this area was also part of the Austrian-Hungarian monarchy with its capital Vienna and it’s so called “Vienna school” of the palaeontology institutions there. Probably this “miss take” of Mojsisovics led to some changed ammonoid zones within the Norian timescale, which last into the 20th century. It was the merit of the Canadian Triassic worker E.T. Tozer to correct this long lasting error by establish his own North American Triassic timescale, based only on North American, mainly Canadian Triassic ammonoid locations. The pelagic (deeper marine) Triassic sedimentation in Austria starts with the uppermost Anisian Flexo-Ptychites beds/lenses of the Schreyeralm limestone. This is also the base of the Hallstatt formation. The next frequent ammonoid lenses/layers occur within uppermost Ladinian/lower Carnian strata in this formation. The lower to middle Ladinian time frame in between was not well documented with ammonoids by the early researchers of the 19th century. At some historical locations the lower Ladinian part is/was given but was not really recognised by them. Later, modern researchers used microfossils to determine the placement of large parts of the grey to violet limestone in the Hallstatt formation into the Ladinian. Within the 20th century also scarce ammonoids were mentioned from these middle Ladinian strata. Fig.3 Anisian Schreieralm limestone with cross sections of Flexoptychites sp. Fig.4 Monophyllites sphaerophyllus (HAUER) from the Schreieralm limestone In general, ammonoid locations are not frequently known within the Ladinian part of the Hallstatt limestone. The most common fossils are Crinoid stem parts, Bivalves and Conodonts. The limestone facies consists of red to grey, sometimes yellowish to grey coloured limestone which is locally interbedded with marls. Also strongly condensed successions are common there and fossils also do not occur in continuous layers. Comparable Ladinian ammonoid faunas are also well known from similar Hallstatt type limestone in Greece and Italy. They show similar ammonoid faunae of Ladinian to Carnian age. In the Tethys realm the whole Ladinium is split into two subdivisions today. Upper Ladinian = Longobardian, Lower Ladinian = Fassanian, The historical zone ammonite of the Longobardian is Protrachyceras archelaus (LAUBE). Fig.5 Protrachyceras archelaus (LAUBE), in MOJSISOVICS “Die Cephalopoden der mediterranen Triasprovinz“ Wien 1882 Tafel XXXL, Fig. 1, But Protrachyceras archelaus LAUBE do occur within a longer time span and is therefore not perfect for stratigraphic aims. The old archelaus zone of the Ladinian was therefore changed into several Longobardian and Fassanian ammonoid zones of today. Within the Tethys realm the Longobardian is split into the ammonoid zones of: Daxatina canadensis Frankites regoledanus Protrachyceras longobardicum The Fassanian is split to the ammonoid zones of: Eoprotrachyceras gredleri Protrachyceras margaritosum Eoprotrachyceras curionii The ammonoids shown in this report come from a condensed fossil bed roughly inserted to the turquoise marked ammonoid zones of the timescale below. Historical Ladinian locations The condensed lower Carnian fossil lenses on the famous historical Feuerkogel show almost all a portion of the upper Ladinian at their base. This is also visible at other Lower Carnian locations within the Hallstatt limestone. During the last years Proarcestes sp. from a new location are sometimes shown for sale in the internet. They are sometimes identified as Arcestes sp. from Norian strata. But it is Proarcestes, therefore its Norian age is definitely wrong. I visited this new locality a few years ago. All locations there are of Ladinian age which is evidenced by Proarcestes cf. subtridentinus, Anolcites sp. and Epigymnites sp. This fauna is maybe slightly younger than the fauna shown later here in this report. Fig.6 Some Epigymnites arthaberi (MOJS.) and Epigymnites moelleri (MOJS.) from the above mentioned location The new location Several years ago a friend and I were lucky to find a hitherto unknown middle Ladinian ammonoid location during a prospecting trip. At this location the normal limestone succession is penetrated by several fractures and tectonic influence across the normal layer direction is also visible there. The fossil layer itself, in which ammonoids were frequent, consists of a very strong condensed upper part of lower Longobardian age, indicated by Protrachyceras longobardicum (MOJS.), and a lower part of a slightly older age indicated by scarce last descendants of Ptychites cf. pauli MOJS. which show deeply incised second and third lateral saddles similar Aristoptychites or Arctoptychites. Therefore the location is ranged by me to the transition of the ammonoid zones of Protrachyceras longobardicum and the underlying Eoprotrachyceras gredleri zone. Outside of the Tethys realm this is roughly comparable to the zones of Meginoceras meginae MC LEARN and Tuchodiceras poseidon (TOZER) of the North American timescale. Both zones are known from the Triassic of British Columbia in Canada too. Tozer, 1994, wrote that flat forms of Protrachyceras sikianum MC LEARN are comparable with Protrachyceras longobardicum (MOJS.) and the thicker morphs of Pt. sikianum MC LEARN with Pt. archelaus (LAUBE). Fig.7 View of the lower, sometimes more greyish limestone part of the fossil layer. The chisel points to a Sturia cf. semiarata MOJS. The furrows on the limestone block have their origin in the strong condensation of this limestone. One can recognize by this feature the underlying part of a condensed limestone (fossil) layer. Fig.8 In contrast to the above shown picture, a view of the underside of the overlaying layer where craters/hollows are visible. These two features can be used for recognizing up and downside in strongly condensed limestone. This feature is independent from the Triassic age of the rock and occurs in condensed limestone of Jurassic age too. The right hanging limestone block contains the fossil layer. Fig.9 Protrachyceras longobardicum (MOJS). in situ. View from the underside. The upper half of the ammonoid was totally dissolved due to the extreme condensation of the uppermost limestone layer at this location. In this location P. archelaus occurs very scarcely. It is no good indicator for stratigraphic aims here at all. A normal collector can use the following features to insert ammonoids into the Ladinian timescale. The frequent occurrence of Proarcestes sp. with a wavy end body chamber is a sign for Ladinian age. All forms of Sturia sp. are restricted to the late Anisian and Ladinian. The occurrence of real Ladinian Protrachyceras MOJS. The following picture will show you the main differences between Protrachyceras, Trachyceras and Neoprotrachyceras. Fig.10 In contrast to Trachyceras the venter furrow of real Protrachyceras MOJS. is bordered by nodes which show a single point per node. Protrachyceras are restricted to the Ladinian. Real Trachyceras show “broader” nodes with two or three points a node bordering the venter furrow. Trachyceras is frequent in the Lower Carnian (Julian) The genus Neoprotrachyceras KRYSTYN looks similar toTrachyceras but shows also just one point per node, sometimes changing up to two points per node within maturity. Neoprotrachyceras is restricted to the uppermost Lower Carnian and lowermost Upper Carnian (e.g. the genus Spirogmoceras SILBERLING in the Dilleri Zone of the North American Tuvalian) For a newbie collector it is difficult to find some fossils in the Hallstatt limestone at all. To place them into the right ammonoid zone is sometimes the easier part of the exercise. Fig.11 A weathered cross section of Proarcestes sp., visible at the limestone wall. Notice the bleached limestone surface in contrast to the colour of the fresh rock. Fig.12 Talus block with visible cross sections of ammonoids and orthocone nautiloids Natural picture size is 20cm. The edges of the fossils are deeply weathered in. This can be a sign that the fossils will probably split out well. Small idiomorphic Biotite crystals up to one mm in size, fine Feldspar crystals and thin greenish tuffitic crusts around some ammonoids and limestone clasts indicate a distant simultaneous volcanic event, adjacent to the palaeo Hallstatt realm. This is the very first observation of volcanic fallout/washout within the Hallstatt limestone column. Within other tectonic nappes in the Northern and Southern Calcareous Alps (Dolomites) volcanic (Tuffitic) ash layers are a frequent feature in Ladinian time. In the adjacent Tirolic nappe some volcanic/tuffitic events are evidenced near the base of the archelaus zone. The middle Ladinian fauna listed below was found at this location. Ammonoidea cf. Beyrichites sp. Eupinacoceras cf. damesi (MOJSISOVICS). Epigymnites cf. ecki (MOJS.) Epigymnites cf. breunneri (HAUER) Epigymnites arthaberi (MOJS.) Gymnites raphaelis TOMMASI Megaphyllites obolus MOJS. Monophyllites wengensis (KLIPSTEIN) cf. Silenticeras sp. Sturia cf. sansovinii MOJS. Sturia semiarata MOJS. Proarcestes ombonii TOMMASI Proarcestes subtridentinus MOJS. Proarcestes .sp. Procladiscites sp. Protrachyceras archelaus (LAUBE) Protrachyceras longobardicum MOJS. Protrachyceras sp. Ptychites cf. pauli MOJS. Ptychites cf. plusiae RENZ Michelinoceras sp. Atractites sp. Syringoceras cf. longobardicus Nautilus div. sp. Bivalves Daonella sp. Peribositra sp. Brachiopoda: Discinisca sp. Austriellula dilatata (SUESS) Important ammonoid species of the archelaus zone A beautiful, conspicuous faunal element of the archelaus zone is Protrachyceras longobardicum MOJS. the zone ammonoid of the Langobardicum Zone This species shows its maximum roughly in the lower middle of the former archelaus zone and can be used well for stratigraphic aims. As mentioned earlier in this report compressed variants of Protrachyceras sikanianum MC LEARN are comparable to Pt. longobardicum MOJS. The thicker variants of Pt. sikanianum rather resemble Pt. archelaus LAUBE. Fig. 13 Protachyceras longobardicum MOJS. with Proarcestes ombonii TOMMASI and Proarcestes cf. subtridentinus MOJS. Fig. 14 Pt. cf. longobardicum, some juvenile Arcestes sp. and the brachiopod Austriellula dilatata. Fig. 15 Epigymnites breunneri (HAUER) and Monophyllites wengensis (KLIPSTEIN) Fig. 16 Epigymnites arthaberi MOJS. and Monophyllites wengensis (KLIPSTEIN) Fig. 17 Gymnites raphaelis TOMMASI Fig. 18Discinisca sp. Looks like a fossil Limpet gastropod (Patellidae) but in reality it is an inarticulate Brachiopoda Fig. 19Sturia cf. semiarata together with Proarcestes cf. ombonii The most frequent faunal element of the Ladinian within the Tethys realm is Proarcestes BRONN. This genus occurs with several species up to Carnian strata. In our location Proarcestes subtridentinus MOJS. and Proarcestes ombonii TOMMASI was often found. The second one can reach the dimension of a small ball. Fig. 20 Proarcestes subtridentinus Fig. 21 Monophyllites wengensis (KLIPSTEIN) In the Hallstatt limestone this genus starts with the Anisian Monophyllites sphaerophyllus via the Ladinian M. wengensis up to the Carnian M. simonyi. Within the descendants of the Triassic Phylloceratida the ancestor of the Jurassic Ammonitida is supposed. Fig. 22 Ptychites cf. pauli MOJS. This species of Ptychites show deeply incised second and third Lateral saddles. I think that this is a feature of allmost all "late" species of Ptychites. Fig. 23 Ptychites cf. plusiae RENZ Fig. 24 Sageceras walteri I hope you have enjoyed this new report about the Ladinian strata of my favourite collecting area. Again I thank, “Danke Roger”, Fossil forum member “Ludwigia” for correcting my “Austrian” English. Kind regards Andreas Literature: ALMA, F. H. (1926). Eine Fauna des Wettersteinkalkes bei Innsbruck. Annalen des Naturhistorischen Museums in Wien, 40, 111-129. BACHMANN, GH, JACOBSHAGEN, V (1974) Zur Fazies und Entstehung der Hallstätter Kalke von Epidauros (Anis bis Karn; Argolis, Griechenland). Z Deutsch Geol Ges, 125: 195-223 DIENER, C. 1900: Die triadische Cephalopoden-Fauna der Schiechlinghöhe bei Hallstatt. Beiträge zur Paläontologie Österreich-Ungarns und des Orient 13 v. HAUER, F. (1888). Die Cephalopoden des bosnischen Muschelkalkes von Han Bulog bei Sarajevo. KK Hof-und Staatsdruckerei. von Hauer, F. (1888. KK Hof-und Staatsdruckerei. KITTL, E., 1908, Beiträge zur Kenntnis der Triasbildungen der nordöstlichen Dobrudscha. Denkschriften der mathematisch-naturwissenschaftlichen Klasse der kaiserlichen: Akademie der Wissenschaften, v. 81, p. 445- 532 KRISTAN-TOLLMANN, E, KRYSTYN, L (1975) Die Mikrofauna der ladinisch-karnischen Hallstätter Kalke von Sakliblei (Taurus-Gebirge, Türkei). Sitzungsber. Österr. Akad. Wiss. Math. Naturwiss. Kl. Abt. I, 184 (8-10): 259-340 KRYSTYN, L. Zur Ammoniten und Conodonten-Stratigraphie der Hallstätter Obertrias(Salzkammergut, Österreich), Verh.Geol. B.-A., Wien 1973 KRYSTYN, L (1983) The Epidauros Section (Greece) – a contribution to the conodont standard zonation of the Ladinian and Lower Carnian of the Tethys Realm. Schriftenreihe Erdwiss. Komm. Österr. Akad. Wiss., 5: 231-258. MOJSISOVICS, E. 1893: Die Cephalopoden der Hallstätter Kalke, Abhandlungen der Kaiserlich-Königlichen Geologischen Reichsanstalt, II Band, Wien 1893 MOJSISOVICS, E. 1896: Beiträge zur Kenntniss der obertriadischen Cephalopoden Faunen des Himalaya, Denkschriften der Kaiserlichen Akademie der Wissenschaften Mathematisch–naturwissenschaftliche Classe, 63, 575–701. Wien 1896, TOZER, E. T. 1994. Canadian Triassic ammonoid faunas. Geological Survey of Canada Bulletin, 467, 1–663. MOJSISOVICS, E. V. 1879. Vorlaufige kurze Übersicht der Ammoniten-Gattungen der mediterranen und juvavischen Trias. Verhandlungen der kaiserlich- königlichen geologischen Reichsanstalt, 1879(7):133–143. MOJSISOVICS, E. V. 1882. Die Cephalopoden der mediterranen Triasprovinz. Abhandlungen der kaiserlich-königlischen geologischen Reichsanstalt, 10, 1–322. NITTEL, P. (2006) Geo Alp, Vol.3, S93-145, Beiträge zur Stratigraphie und Mikropaläontologie der Mitteltrias der Innsbrucker Nordkette(Nördliche Kalkalpen Austria) PISTOTNIK, U. 1973-74 Fazies und Tektonik der Hallstätter Zone von Bad Ischl — Bad Aussee (Salzkammergut, Österreich) RENZ, C. – 1931 Die Bulogkalke der Insel Hydra, Ostpeloponnes RENZ, C. (1910): Die mesozoischen Faunen Griechenlands I. Die triadischen Faunen der Argolis, Palaeontographica 58, S. 1-103, Tab. 1-7, Fig. 15 RENZ, C. Neue griechische Trias Ammoniten aus den Verhandlungen der Naturforschenden Ges. Basel. S. 218- 255, Tab. 6-8, Abb. l, Basel. SALOPEK M. 1911,Über die Cephalopoden der mittleren Trias von Süddalmatien und Montenegro, Abhandlungen der .k.k geol. Reichsanstalt, Band 16, Heft 3 WEITSCHAT, W. & LEHMANN, U. Stratigraphy and ammonoids from the Middle Triassic Botneheia Formation (Daonella Shales) of Spitsbergen With plates 1-6, 2 tables and 9 text-figures Mitt. Geol.-PaläonInst. Univ. Hamburg. Heft 54, S. 27-54 WENDT, J. (1970) Stratigraphische Kondensation in triadischen und jurassischen Cephalopodenkalken der Tethys. N. Jb. Geol. Paläont. Mh., 1970/7: 433-448

I am happy because I ve just finished prep work of an upper Carnian ammonoid block. The block was found in spring this year (2013). It was prepared from the downside. Prep time is about 40 hours. First pic is the rough block. It looks unspectacular because it was a dry day and the real colours of the limestone can not be seen. After washing its red and grey colour is visible. During prep work I took of some limestone parts and ammonoids to reach the fossils below. Unfortunly a fault runs through the block. You can see the dislocation of the bigger horizontal laying orthocone nautiloid. Therfore the uppermost ammonoid and the small nautiloid nearby needed a little restauration. (resplit, dislocate and glue again) The block shows a typical tethydial ammonoid fauna of the uppermost aonoides zone/Carnian/Upper Triassic. On the backside of the slab the marly horizon of the uppermost Julian, Carnian Pluveal Event starts.

Last Wednesday was a sweltering 94 degree high humidity day. I had an appointment in the area and couldn't help checking out a favorite site; the Dave Elliot bed on Route 209 just west of Kingston, NY. The bed is highly fossiliferous silty sandstone, just a few inches thick in an exposure that's 30 to 40 feet high. The bed is Middle Devonian age with tiny bivalves and cephalopods dominant. I spent a total of three hours chipping away hunks of rock from the crumbly cliff and had my best day there so far: seven complete or nearly complete goniatite ammonoids, Tornoceras mesopleuron. a three and a half inch nearly complete straight-shelled nautiloid, Michelinoceras sp.?, five Eumetabolotoechia brachiopods (normally I just find one or two per day), a tiny spiriferoid brachiopod (unidentified) I've never found at this site before, bivalves, Nuculites sp.?, the twig of a fossil plant, and two other unidentified fossils. The day was well worth it, despite the heat. The unidentified fossils I'll show Dr. Bartholomew, professor of paleontology and stratigraphy at the State University near where I live. Dr. Bartholomew is doing an extensive study of the Dave Elliot Bed in eastern New York. The Dave Elliot fauna here in Kingston is similar to the fossils from Hannacroix Ravine except that brachiopods are rarer at Hannacroix. The presence of well preserved fossil plants in marine sediments would suggest the presence of a nearby river that carried their remains from some terrestrial habitat. The absence of corals and relatively low species diversity also suggests the water contained a large ammount of sediment making it hospitable to only those creatures who could adapt to this cloudy environment. Finding fossils, especially cephalopods, and speculating on what the prehistoric environment was like is a great source of fascination for me. I try to get there whenever I have a chance. Less than a mile north of here, also on Route 209 is another even older Middle Devonian fossil bed that produces abundant spiriferoid brachiopods and rugose corals, and about a mile and half west is a site where spirifers and occasional bivales and cephalopods can be found.

Last weekend I did hunt again in the Austrian mountains. While prospecting a Triassic area I found a little fossil lense containing a small Upper Triassic/ Carnian/Tuvalian ammonoid fauna. It contain several Tropites sp., Trachysagenites, Metatirolites, Polycyclus, Megaphyllites and Projuvavites in rather small but very well preserved specimen. At first I found a small talus stone with ammonoids at the flat part of a slope/cliff. It shows a Trachysagenites sp.(2.5cm) Then I searched from this point straight upwards the hill and found a small fossil lense in Tuvalian limestone. I found it in an unexpected position. I think I have to go back and search the area closer. Maybe there is a second fossil lense in this area because the feature of the fallen block looks a little different compared to the feature of the fossil lense. But both are of the same time. Two times luck at one day! Andreas

Some tiny ammonoids from the Finis shale at Jacksboro, TX. I'll try them again with the microscope at a later time. They are hard to work with this small.

Last weekend I started my collecting season 2013 after this long winter. I was fortunate and found some Lower Carnian ammonoids. Hunting again is a very good feeling.

Last week my friend and I went to our probably last trip this year before winter comes. We went to an old location of mine. I stopped digging there years ago because rock was the more solid the deeper we dug. Now after several winters I hoped for new material. We found less but good material. I did preparation immediatly after washing . The ammonoids are of upper Triassic, lower Carnian age. Exactly they range into the Zone of Trachyceras aonoides(=Zone of Trachyceras desatoyense in US strata) Sorry for the bad pics but light was/is not good in these grey, misty days. Andreas

Hello Yesterday I started my Triassic ammonoid hunting season 2012. The weather was pretty cool and windy but no rain. Snow was just gone at this location. I found a few Norian ammonoids at the beginning of my trip and some small blocks with Carnian ammonoids on my way/search back to my car. They show a small, but fine preserved, ammonoid fauna of the Tuvalian stage(uppermost Carnian/upper Triassic) regards Andreas

The Tuvalian Substage Of The Triassic Hallstatt Limestone In Austria Written by Andreas Spatzenegger Dear Fossil Forum members! This report will introduce you to the Tuvalian substage (uppermost Carnian/ Triassic) of the so called Hallstatt limestone in Austria. View above the Hallein-Berchtesgaden Triassic area to the Watzmann and the Hochkalter mountains. The name of this substage was chosen by "Old master" Mojsisovics from the mediaeval name of the hill ridge/salt mine area between the rivers Salzach and Königseeache in the borderland between Bavaria (Germany) and the county of Salzburg (Austria). Originally this term was of Roman source (Mons Tuval) but it was preserved in this area to our days (e.g. ruin of the castle Tuval) The wordTuval has probably Hebraeic roots and mean "rich" or "blessed" earth because of the saltmines of this area. The ammonites of the family Tropitidae (Mojsisovics 1875) are characteristic for the whole Tuvalian. Typically important genera of this family are: Discotropites, Gymnotropites, Margaritropites, Paratropites, Pleurotropites and Tropites s. s. A few other genera not listed above belong also to this family but I will not list them here because this report should not get too long. Representative for the Tropitidae is shown a picture of Tropites subbullatus, the zone ammonite of the alpine Tuvalian II, from the old Monographic work of Mojsisovics „Das Gebirge um Hallstatt. 1893, Taf. CVI," Tropites subbullatus (Fr. v. Hauer) 1849 Division of the Tuvalian In the North American literature (after Tozer) the Tuvalian is split into three Zones. It starts with the Dilleri Zone, the Welleri Zone and the Macrolobatus Zone on the top. Characteristic for the Dilleri zone is the arising of the genus Tropites together in co-existence with later members of the genus Neoprotrachyceras sp.(Spirogmoceras SILBERLING) In the Welleri zone Neoprotrachyceras sp. disappear and Tropites becomes a very common faunal element. The Macrolobatus zone is named after Klamathites macrolobatus an endemic ammonite of the North American strata. Other genera of this zone are comparable to the time frame of the latest Tuvalian and the earliest Norian of the Alps. In the Hallstatt (Tethys) realm the following Division is made. Dilleri Zone= Tuvalian I (literature gives little evidence for this zone) Subbullatus Zone = Tuvalian II (corresponds in most parts to the north American Welleri Zone) Anatropites Zone= Tuvalian III (corresponds in parts to the North American Macrolobatus Zone) In the Alps normally you can observe in the field only Tuvalian II and Tuvalian III, but one has to ask the question if there are all three North American Zones included in these two alpine Zones. In my opinion there is less evidence for a time gap in the lower Tuvalian of the Alpine strata. Visibly stronger condensation in this generally condensed limestone occurs frequently in the upper Tuvalian III. E.g. Discotropites sandlingense is in North America a clear Dilleri faunal element but in the Alps it is ranged into Tuvalian II (Welleri Zone). The same is done with the genus Traskites sp. (corresponding to alpine Sandlingites sp.). Some ammonites of the upper part of the Macrolobatus Zone are also ranged to the first zone of the alpine Norian stage. I think the correlation of the North American scheme with the Alpine scheme probably doesn't fit exactly. It is very difficult to range a Tuvalian fauna exactly. Probably Tuvalian 1 is recognizable in the Alps only by the composition of the faunal spectrum (the quantity of some special genera). In some „lenses", Trachysagenites sp. Sagenites inermis, Sandlingites sp. occur very frequently together with scarce Tropites sp. and Sirenites sp. and with very rarely Neoprotrachyceras cf. thyrae. Therefore it seems important to me to get a survey of a Tuvalian fauna in a lens or fissure filling. A good way to do this is to write a fossil list of each block found. The best way, in my opinion, is to prep out and expose as many ammonoids as possible and leave them on the block. In this way one can recognize later possible errors and study the sedimentary features of this block. Marking down and upside should be done if possible. Even on small pieces you can recognize a current setting with this method. A small slab (6cm) with some current deposited Pamphagosirenites sp.(Tuvalian 2) The transition (proved with ammonoids) from Tuvalian to the Norian is confirmed by science only in one location in the Hallstatt limestone. This bedded profile of a Tuvalian fauna which is overlain by a Norian fauna comes from the "Feuerkogel". In this abandoned, fully filled place the lower transition from the Julian to the Tuvalian was also evident in parts. The next Picture shows the geologic transition of the Carnium/Norian border from another area. Between Carnium and Norium are some lenses of a strongly condensed limestone bed which yield ammonites of the late Tuvalian. The latest Tuvalian and lowermost Norian are confirmed there only by microfossils. The rock wall at this place consists of grey limestone which begins in the aonoides/austriacum zone. Scarce ammonite lenses in this limestone point to the Tuvalian 1. In the Tuval ranged area the limestone succession is bedded as in the Norian part. In the Tuvalian part of the picture a bedding angle as in the Norian part of the picture is visible. The Tuvalian marked succession consists of a sparitic, biotic rich limestone with interfaced Halobia beds. In my opinion this is a larger area of an internal bedded lens/hollow rather than a fissure filling. Discotropites plinii, Tuvalian III, from the above shown Carnian/Norian transition There exist/existed four classic historical locations within the Hallstatt limestone which yield a Tuvalian ammonite fauna The historical location on the Millibrunnkogel/Vordersandling, the historical Tropites location on the Raschberg and the „Tuval" area round about Hallein/Berchtesgaden. The latest newly discovered location (at the beginning of the 20th. Century) was the Tropites location on the world famous Feuerkogel. The whole area there is a strictly protected place and the locations there are buried under tons of collecting debris. Within the last hundred years of Triassic research in the Alps no new Tuvalian location was discovered. This fact shows how really scarce ammonite bearing Tuvalian rock occurrences are in the Hallstatt limestone. Tuvalian fauna collected at the location "Vordersandling". Size of the embedded Tropites sp. is 1cm. Fragments of Tropites sp. found at the historical location on the Raschberg. Size of the Tropites shell parts ca. 2cm Block with Tuvalian fauna from the Hallein/Berchtesgaden area. Size of the Pinacoceras rex at the left on the Block is 6cm Basinal layers/beds of the Tuvalian After the Julian Aonoides/austriacum beds (lenses) a distinct ammonite faunal change appears in the following Tuvalian. Most of the dominant Julian genera disappear at the uppermost Julian. In the Tuvalian roughly 20 new ammonoid genera appear. One trigger for this big faunal change in the Tethys realm was the Carnian Pluvial Event (Reingraben Event). The lenses and layers of the aonoides and austriacum zone were deposited during this time span on the Hallstatt deep swells. A possible (in controversial discussion) rise in temperature of the seawater column at the end of the Julian was the last step of the faunal change. The last subzone of the Julian is the so called „Sirenites horizon" which is difficult to recognize and determine. Sirenites sp.2cm from a possible transition level between Julian and Tuvalian Deformed part of the fossil lens where this fauna comes from. Visible is the plastic deformation of the rock which resulted from motions in an early diagenetic phase. Small slab collected at this lens. Beside frequent Sirenites sp. and Arcestes sp., Megaphyllites and Neoprotrachyceras are visible. I found a fissure filling of clear Julian age in a tectonically stressed limestone succession below this above mentioned limestone. Remarkable in this location was a clear preponderance of Arcestes sp. which differentiates this location from other Julian locations where normally Joannites sp. is the dominant leiostrake (ammonoids with a smooth shell) genera. Sageceras haidingeri from this above mentioned Julian location with the preponderance of Arcestes. Tuvalian Sometimes historical literature speaks of the beds with Tropites subbullatus. This feature is often close to my own impressions. In the case of ammonite bearing limestone, nearly the same Lithology is visible at all different locations. Mostly a succession of grey to red limestone beds which include bivalve beds, rough sparitic and biogenic layers can be observed. Embedded in this succession are fissures and lenses yielding ammonites in micritic fillings. The faunal compositions of each ammonite lens in this limestone succession changes slightly depending on the level within the succession. Generally the embedded ammonites are mostly small and often of a spherical form. Therefore it is difficult to recognise if it is a real fissure filling or a lens (because of the lens shaped cross section). Piece from a „fissure filling" with Trachysagenites erinaceus on the top Some of you may ask where the difference is. The most important feature of a lens is the recognition of a nearly normal deposition in which the lens is embedded. In clear fissure fillings this is not given. A fissure can strike through several much older layers in every concievable way and angle. So it is a matter of fact that all transitions between lenses and fissures are also possible. One can imagine that it is often the personal impression of an author which tends to decide. In the case of talus blocks it is nearly impossible to determine whether a lens or fissure is given because the lateral transition is mostly lacking. Tuvalian talus block. Fissure filling or lens? . Tuvalian deposits in which bedded ammonite layers are visible occur very scarcely. The ammonites within are mostly bigger and often preserved with body chamber. The typical hash feature of other Tuvalian lenses is lacking there. The ocean current and the composition of the paleo seafloor lead to the different deposition of the Tuvalian locations. If one looks carefully one can imagine the direction of the paleo current in the following picture. Most apertures of the ammonites look downwards and the small orthicone ammonoid points in the direction of the paleo current. This untypical Tuvalian fossil slab with Tropites torquillus (big ammonite) was found in a big lens/layer location. Prep work was done from the lower side. The high biotic parts of normal Tuvalian rock are mostly lacking in such big lenses. The ammonites at this location are dissolved on the upper side and were embedded in a strongly condensed limestone succession which laterally runs out after several meters. Also the ammonites were bigger and preserved with body chamber in such big lenses. Some layers are enriched with crinoid stem fragments. Rock from above mentioned location with a visible curve of an ammonite. Tuvalian slab showing a juvenile Discotropites sandlingense from a typical Tuvalian hash lens. How to find the historical locations? Searching for old locations in historical literature has its own thrill. Finding such spots after having completed preparatory research is a very pleasant and pleasing experience. I found the historical location on the Raschberg Mountain, which was unknown to me, years ago after a long search in the field. The old location was only visible through a small man made hollow on the ground which was only discernable with a large amount of fantasy. Because of the fitting of the surrounding limestone with other Tuvalian locations known by me, I looked closer and thereby discovered it. Such adventures make geological history alive and one gets plenty of experience and knowledge. Old hand-made drilling hole at an historical Tuvalian location. This is visible by the oval cross-section of the hole, which was created by the continual pendulating of the driller-chisel by hand. Smaller pieces can still be found at the historical locations. But only when the location is well known and when one is willing to hike for a few hours. The most important rule for collecting this limestone is the fact that there are no rules! Everything is possible. The whole Tuvalian can be only a few meters thick at one point and then a few steps farther on its thickness can multiply enormously. Thickening and thinning out of limestone beds within very short distances are the normal case. The paleo relief of this former Triassic ocean floor was too narrow spaced and too differentiated for the deposition of an undisturbed succession of limestone. Therefore a correct stratigraphic succession exists only on paper. This was a modest view into my special world of collecting. I hope you enjoyed reading it. I thank Fossil Forum member Ludwigia for correcting my uncivil kind of English. Regards Andreas Literature: KRYSTYN, L. Zur Ammoniten und Conodonten-Stratigraphie der Hallstätter Obertrias(Salzkammergut, Österreich), Verh.Geol. B.-A., Wien 1973 KRYSTYN, L. und SCHLAGER, W., 1971 : Der Stratotyp des Tuval. — Annales Inst. Geol. Publ. Hungarici,. 54(2), 591-605, 5 Abb., Budapest MOJSISOVICS, E. 1893: Die Cephalopoden der Hallstätter Kalke, Abhandlungen der Kaiserlich-Königlichen Geologischen Reichsanstalt, II Band, Wien 1893 TOZER, E. T. 1994. Canadian Triassic ammonoid Faunas. Geological Survey of Canada Bulletin, 467, 1–663. The Global Triassic.- New Mexico Museum of Natural History and Science Bulletin, 41, 59-67. ... Hornung, T., Spatzenegger, A. & Joachimski M.M. (2007): Multistratigraphy of condensed ammonoid beds of the …